Geological Quarterly, 2019, 63 (1): 178–191 DOI: http://dx.doi.org/10.7306/gq.1457 Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue Assimina ANTONARAKOU1, *, George KONTAKIOTIS1, Aristomenis P. KARAGEORGIS2, Eva BESIOU1, Stergios ZARKOGIANNIS1, Hara DRINIA1, Graham P. MORTYN3, 4 and Efthymis TRIPSANAS5 1 National and Kapodistrian University of Athens, Faculty of Geology and Geoenvironment, School of Earth Sciences, De- partment of Historical Geology-Paleontology, Panepistimiopolis, Zografou, 15784, Greece. 2 Hellenic Centre for Marine Research, Institute of Oceanography, 46.7 km Athens-Sounio Avenue, 19013 Anavyssos, Greece 3 Universitat Autànoma de Barcelona (UAB), Institute of Environmental Science and Technology (ICTA), Edifici Z Carrer de les Columnes, Bellaterra 08193, Spain 4 Universitat Autànoma de Barcelona (UAB), Faculty of Geography and History, Montalegre, 6, 08001 Barcelona, Spain 5 Hellenic Petroleum Exploration and Production of Hydrocarbons S.A., 4A Gavrias, Marousi, Spain Antonarakou, A., Kontakiotis, G., Karageorgis, A.P., Besiou, E., Zarkogiannis, S., Drinia, H., Mortyn, G.P., Tripsanas, E., 2019. Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico ana- logue. Geological Quarterly, 63 (1): 178–191, doi: 10.7306/gq.1457 Associate editor: Wojciech Granoszewski This study combines high-resolution planktonic foraminiferal eco-biostratigraphy and palaeoclimatic data from the high-sedi- mentation-rate core JPC-26 from the northwestern margin of the Gulf of Mexico (GoM). The eco-biozones recognized (GOMPFE1-12) being correlated with published Mg/Ca-based sea surface temperatures. This updated palaeoclimatic and stratigraphic reference record facilitates correlations with the Greenland ice core events and their climatic relationships, and also provides a solid stratigraphic framework for correlations with other palaeoclimatic and palaeoceanographic records in the circum-GOM/Caribbean region. This multidisciplinary approach underlines the utility of supporting conventional dating methodologies with different constraints, and further reveals a powerful tool for reliably correlating marine records between comparable deep-sea marginal settings and coeval sequences of this region. Key words: integrated stratigraphy, Late Glacial–Holocene transition, planktonic foraminiferal eco-bioevents, deep-sea sedi- mentary correlations, climate variability, palaeoceanography. INTRODUCTION North Atlantic region (Wang and Enfield, 2001), and therefore acts as a key regulator of subpolar North Atlantic oceanography and climate in Europe. In particular, the GoM is a key area for In the last half-century, considerable interest has developed global thermohaline circulation (THC), global heat exchange regarding the role of the (sub)tropical oceans in climate change, and climate system (Broecker, 1991), because its hydrographic and in particular, oceanic sub-basins and marginal seas that characteristics (high sea surface temperature (SST) and salin- are often more responsive to palaeoceanographic and palaeo- ity (SSS) values) partly control Gulf Stream physical properties. climatic changes than to broader global ocean basins, because Its small volume, compared with major ocean basins, causes of their smaller size and partial isolation (Marino et al., 2009; changes in its climatic forcing to be recorded virtually instanta- Kontakiotis et al., 2013; Kontakiotis, 2016). As an example, the neously in palaeoceanographic proxy data such as stable iso- tropical Western Hemisphere Warm Pool (WHWP), which en- topes, geochemical ratios, and microfossil abundances. More- compasses the Caribbean Sea and the Gulf of Mexico (GoM), over, the direct influence of North Atlantic surface water on the is an important heat and moisture source for climate in the faunal assemblages gives a measure of the close hydrological relationship between the North Atlantic and the GoM water masses, and underlines the prominent role of the GoM in the understanding of global climatic evolution (Thirumalai et al., * Corresponding author, e-mail: aantonar@geol.uoa.gr 2018). Due to its latitudinal position, the semi-enclosed character, Received: November 2, 2018; accepted: January 31, 2019; first published online: April 1, 2019 the high sedimentation rates and close atmospheric and oce- Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue 179 anic connections with the North Atlantic region, the GoM is palaeoclimatic and stratigraphic reference record, facilitating among the most studied marginal basins. In particular, the inter- correlations with the Greenland ice core events and their clima- play between Mississippi River discharge, the open ocean wa- tic relationships, and also providing a solid stratigraphic frame- ter masses and atmospheric circulation creates a complex and work for correlations with other palaeoclimatic and palaeo- dynamic system responsible for hydrological fluctuations on ceanographic records in the circum-GoM/Caribbean region. both annual and long-term timescales. To better understand the impact of these parameters on the regional climate, a number of studies based on various marine proxies has focused on the OCEANOGRAPHIC SETTING hydrologic evolution of the basin during the late Quaternary (Metcalfe et al., 2000; Aharon, 2003, 2006; Poore et al., 2003; The GoM is a semi-enclosed oceanic basin on the south- Flower et al., 2004; LoDico et al., 2006; Nürnberg et al., 2008; eastern margin of North America that covers an area of Ziegler et al., 2008; Richey et al., 2011, 2012; Spear et al., 1,555,000 km2 (Fig. 1). It is connected to the Atlantic Ocean by 2011a; Rasmussen and Thomsen, 2012; Limoges et al., 2014; the Florida Strait (FS) and to the Caribbean Sea by the Yucatan del Monte-Luna et al., 2015; Antonarakou et al., 2015; Shakun Channel (YC; INEGI, 2014). Its hydrographic properties result et al., 2016; Reynolds et al., 2018). However, the reconstruction mainly from the interplay between the open ocean water of the variability of late Quaternary climate needs detailed masses, Mississippi River discharge, and atmospheric circula- eco-litho-chronostratigraphic control (Triantaphyllou et al., tion. The surface circulation in the GoM is known to be a key ele- 2009; Siani et al., 2010; Drinia et al., 2016; Koutrouli et al., ment in the North Atlantic and the Atlantic Meridional Overturning 2018). In this respect, notable contributions are required from Circulation (AMOC), as it conveys heat and salt from low to high micropaleontological, biogeochemical, and sedimentological latitudes via the Gulf Stream; it is largely influenced by: (1) the studies. In particular, morphological and compositional chan- energetic Loop Current (LC) and its associated eddy field ges in the planktonic foraminiferal assemblages recorded in (Ohlmann et al., 2001; Morey et al., 2003b; Liu et al., 2012; marine sediments and/or the water column provide detailed in- Gopalakrishnan et al., 2013; Schmitz et al., 2013; Weisberg and formation on the physical and chemical properties of the sur- Liu, 2017) in the eastern part, and (2) a less prominent west-flow- rounding water masses and their relationships with climatic ing anticyclonic gyre that moves on to the western part of the ba- variability (Renaud and Schmidt, 2003; Schmidt et al., 2004a, b; sin, varying appreciably in intensity with season and location Spear et al., 2011b; Kontakiotis et al., 2011, 2013, 2016a; (Behringer et al., 1977; Müller-Karger et al., 1991; Zavala-Hi- Thirumalai et al., 2014; Antonarakou et al., 2015; Jonkers et al., dalgo et al., 2006; Putrasahan et al., 2017). The most prominent 2015; Kontakiotis, 2016; Arellano-Torres and Machain-Castillo, surface circulation feature in the GoM, the LC, brings warm and 2017; Reynolds et al., 2018; Wilson et al., 2018). For instance, it salty tropical waters originating from the Caribbean Sea through has been suggested that planktonic foraminifera alter their the YC into the GoM, loops northwest, and exits into the North shape and size, which determine their weight and their overall Atlantic Ocean through the Florida Straits (Florida Current – FC), density in direct response to changes in water density and vis- and eventually feeds the Gulf Stream (GS; Fig. 1; Elliott, 1982; cosity to retain or modify their hydrodynamic behaviour accord- Blumberg and Mellor, 1985; Hofmann and Worley, 1986; ingly (Caromel et al., 2014; Zarkogiannis et al., 2019a, b). Un- Jochens and DiMarco, 2008; Auladell et al., 2010; Oey et al., derstanding the drivers of these changes, along with the impli- 2013). The latitudinal extension of the Caribbean water inflow cations for changes in biogeochemistry and climate, is key to (Caribbean Current, CC) into the basin is seasonally modulated understanding the past hydroclimate. They also allow the defini- by changes in the position of the Intertropical Convergence Zone tion of a detailed sequence of regional eco-bioevents for the (ITCZ; Poore et al., 2004, 2005; Nürnberg et al., 2008; Ziegler et late Quaternary (e.g., temporary appearance or disappearance, al., 2008). Northward migration of the ITCZ during the boreal or significant relative abundance variations of specific taxa; Wil- summer causes the LC to propagate farther north, influencing son, 2012), reflecting climatic oscillations, that represent an im- the hydrological properties of the entire basin (temperature, sa- portant tool for accurate subdivision of the late Quaternary linity, wind direction), and finally creates drier conditions during stratigraphic record and facilitate correlations between sites in the boreal winter and rainy conditions during the boreal summer the different sub-basins. The presence of distinct temporal (Saha, 2010). Apart from the distinct role of the LC, fluvial fresh- Quaternary organic-rich zones (ORZ; Tripsanas et al., 2013) in water discharge (mainly the Mississippi River system) directly af- GoM successions represents an additional, independent tool fected by the prevailing precipitation patterns and climatic condi- for dating and correlating marine sedimentary archives. They tions (Montero-Serrano et al., 2010, 2011) also influences the provide isochronous marker horizons that can be correlated via GoM surface hydrography, by modifying the SSS, and by im- geochemical fingerprinting with well-dated meltwater flooding pacting to some extent the thermocline circulation via the GS events (Tripsanas et al., 2007; Meckler et al., 2008; Sionneau et (Aharon, 2003; Morey et al., 2003a; Flower et al., 2004). More- al., 2008; Montero-Serrano et al., 2009; Sionneau et al., 2010; over, the large seasonal loadings of freshwater, inorganic and or- Vetter et al., 2017). ganic matter, and nutrients maintain the northern GoM as an ac- In this work we refine and extend previous biostratigraphic tive ecosystem with dynamic physical and biogeochemical pro- schemes for the area investigated (Kennett and Huddlestun, cesses, such as interactions of eddy cyclone-anticyclone pairs 1972; Kennett et al., 1985; Flower and Kennett, 1990; Martin et with the water column, bottom topography, increased offshore al., 1990) and further highlight the stratigraphic relationship be- productivity, and advection of shelf material into the central Gulf tween foraminiferal and climatic events since the late glacial pe- (Biggs and Müller-Karger, 1994; Toner et al., 2003; Wawrik et al., riod. We report a high-resolution planktonic foraminiferal quan- 2003; Corbett et al., 2004; Luo et al., 2016; Chen and Hu, 2017). titative distribution pattern, and further correlate the eco- In the modern climate system, GoM mean annual SST is bioevents recognized with Mg/Ca-based SST results ~25.85°C with large seasonal amplitude (~8.5°C), whereas sa- (Antonarakou et al., 2015). As a result, this updated and com- linity varies from about 34.4 to 36.3 psu (Antonov et al., 2010; prehensive reconstruction can be considered as a useful Locarnini et al., 2010). 180 Assimina Antonarakou et al. Fig. 1. Bathymetric map of the Gulf of Mexico (GoM) show ing the core location and the main patterns of the surface circulation (white arrows, solid circles) The top-right inset shows the names of the main currents, as described in the text MATERIAL AND METHODS LITHO-CHRONOSTRATIGRAPHY OF MARINE SEDIMENT CORE JPC-26 The sedimentary record of the uppermost 3 m of JPC-26 CORE SELECTION was sampled at 2–5 cm intervals, and consists of three distinct lithostratigraphic units (I–III). The upper unit I (0–1.52 m) con- Core JPC-26 (1995 m b.s.l.) was recovered from the north- sists of reddish-brown to pale yellow hemipelagic mud, and the western continental slope of the GoM (26°22.44’N, sporadic presence of manganese-rich, dark brown mud hori- 92°01.62’W) at a depth of 1995 m (Fig. 1), during the R/V Knorr zons (3 cm thick; in intervals 0.10–0.32 m and 0.45–0.60 m). In 1998 cruise, using the Woods Hole Oceanographic Institution unit II (1.52–1.90 m), hemipelagic muds were intercalated with jumbo piston corer. The core is located offshore of the former three organic-rich zones (0.60–0.95% Corg) slightly (ORZ I) or mouth of the Mississippi River within the Bryant Canyon area, intensely (ORZ II, III) bioturbated (Tripsanas et al., 2007). Their which is represented by a network of intraslope basins sepa- downcore transition to pale greenish-grey hemipelagic muds of rated from each other by sills/plateaus (Tripsanas et al., 2007). unit III (1.90–3 m) is characterized by the presence of two or- The upper 3 m of the core analysed represents an uninter- ganic-rich (0.75–1.30% Corg) reddish-brown (RT) and dark rupted last glacial to Holocene interval, including the Last Gla- green (GT) mud turbidites. The chronostratigraphy of JPC-26 is cial Maximum (LGM) event, and the last glacial termination pe- based on eight accelerator mass spectrometry radiocarbon riod (T1). This core is also characterized by a Holocene thick- (AMS 14C) dates, supplemented by additional tie-points derived ness of 1.5 m that can offer a time resolution on the order of a from the determination of both the isotopic and faunal profile few hundred years per sample step. The Late Quaternary pro- (Antonarakou et al., 2015). vides the best time interval for this research because sea level history is well constrained temporally; moreover, centennial to millennial scale chronostratigraphic resolution is highly achiev- MICROPALAEONTOLOGICAL ANALYSES able through planktonic bio-ecozonation, while palaeoclimate history is best constrained through previously integrated For detailed quantitative micropalaeontological analysis, we sedimentological, micropalaeontological, stratigraphic and picked specimens of planktonic foraminifera from about 15 g of palaeoclimatic studies (Poore et al., 2003; LoDico et al., 2006; dry marine sediment, taken every 2–5 cm along the core. All the Montero-Serrano et al., 2009, 2010; Williams et al., 2010; Ras- sediment samples were washed with running water through a mussen and Thomsen, 2012; Tripsanas et al., 2013; Limoges 63 µm sieve. After washing and drying at 50°C, the samples et al., 2014; Antonarakou et al., 2015; Arellano-Torres and were sieved and the >125 µm size fraction was split with an Otto Machain-Castillo, 2017). micro-splitter into aliquots, from which at least 300 specimens Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue 181 Fig. 2. High-resolution SEM photomicrographs of the planktonic foraminiferal species most indicative for the present study in core JPC-26 A – Orbulina universa; B – Sphaeroidinella dehiscens; C – Globogerinella aequilateralis; D – Globigerina bulloides; E – Globigerinoides ruber sensu stricto; F – Globigerinoides ruber sensu lato; G – Globigerinoides sacculifer; H – Neogloboquadrina dutertrei; I – Pulleniatina obliquiloculata; J – Globorotalia inflata; K – Globorotalia crassaformis; L – Globorotalia scitula; M – Globorotalia menardii; N – Globorotalia tumida; O – Globorotalia truncatulinoides of planktonic foraminifera were picked, identified and counted of the SST variations was constructed based on the down-core using morphospecies-specific and/or specialized taxonomic variation of planktonic foraminiferal abundances, and it was re- references (Kennett and Srinivasan, 1983; Hemleben et al., ferred to as the Planktonic Palaeoclimatic Curve (PPC). The 1989; Kontakiotis et al., 2017). The number of planktonic PPC was obtained by the formula (w – c) ´ 100/(w + c), where: foraminifera counted is statistically reliable for both eco- w represents the warm-water indicators and c the cold water in- biostratigraphic and palaeoclimatic reconstructions (Patterson dicators (Rohling et al., 1993; Kontakiotis, 2016). For and Fishbein, 1989; Capotondi et al., 1999; Drinia and palaeoclimatic interpretation, the PPC record was further com- Antonarakou, 2003; Sprovieri et al., 2003; Sbaffi et al., 2004; pared with previously published SST proxy data (d18O, Mg/Ca) Budillon et al., 2009; Triantaphyllou et al., 2009; Siani et al., from the same or nearby cores (Flower et al., 2004; Ziegler et 2010; Drinia et al., 2016; Bonfardeci et al., 2018). All the speci- al., 2008; Williams et al., 2010; Rasmussen and Thomsen, mens identified showed very good levels of preservation, with 2012; Schmidt et al., 2012; Tripsanas et al., 2013; Antonarakou no traces of dissolution or damage found in the tests. Raw data et al., 2015; Arellano-Torres and Machain-Castillo, 2017). were transformed into percentages of the total abundance and relative percentage abundance curves were plotted, after ex- clusion of rare species (<3%; Globigerinoides conglobatus, RESULTS Globigerinella calida, Globigerinoides tenellus, Hastigerina pelagica, Globorotalia ungulata) and grouping of species with SEDIMENTATION RATES phylogenetic affinities and similar ecological characteristics (e.g., Globigerina bulloides and Globigerina falconensis were Within the GoM, Bryant Canyon is exceptional in that rapid grouped in G. bulloides gr., Globigerinoides trilobus and sedimentation sustained by high rates of terrigenous sediment Globigerinoides sacculifer in G. sacculifer gr., Globigerinella delivery and surface marine productivity makes this basin an aequilateralis and Globigerinella calida in the G. aequilateralis excellent recorder of palaeoenvironmental and palaeoclimatic gr., Globorotalia menardii and Globorotalia tumida in conditions. Sedimentation in the basin is mainly hemipelagic G. menardii gr., and Neogloboquadrina pachyderma and and is strongly linked to the Mississippi River detrital supply Neogloboquadrina dutertrei in neogloboquadrinids respec- (Bouma et al., 1985). This type of deposition is due to the rise of tively). The planktonic foraminiferal relative distributions are sea level that led to the confinement of river-sourced sediments also used as a first-order estimate of SST variations. An index to the continental shelf, and the prevalence of hemipelagic sedi- 182 Assimina Antonarakou et al. mentation over the continental slope of the northwestern GoM. G. bulloides and neogloboquadrinids, whereas warm water The sediment record here investigated spans the interval from species are restricted in these faunal assemblages. The the LGM and the subsequent transition (T1) into the late Holo- palaeoclimatic curve shows relative high variability upcore from cene (i.e. 0–21 ka; Antonarakou et al., 2015) with an average 2.31–1.52 m (19.0–13.0 ka), displaying a characteristic pattern sedimentation rate (SR) of 13.5 cm/ky, which is in agreement corresponding to deglaciation. The warm (~50–60%) interval with prior studies (Leventer et al., 1983; Aharon, 2003; Poore et 2.31–1.90 m (19.0–15.8 ka) is followed by a significant cooling, al., 2003; LoDico et al., 2006; Tripsanas et al., 2007). Sedimen- as reflected by the abrupt drop to glacial values (~20%). The tation rates of each unit reveal a strong down-core increasing rises towards more positive values in the PPC correspond to trend, with the higher SR occurring during the glacial section pronounced deglacial warming peaks (MWFs of Aharon, 2003). (unit III; 18.18 cm/ky) and the deglacial meltwater pulses (unit II; The brief rebound to slightly lower values around 60% at 13.29 cm/ky). Lower SR occurred during the Holocene interval 12.5 ka is related to the Greenland Stadial 2 (GS-2)/Younger (unit I; 11.44 cm/ky) and is consistent with other observations of Dryas (YD) cooling event, and therefore, despite the lower reso- reduced sedimentation rates after 13 cal ka BP (Williams and lution of this part of the core, we can suggest that the transition Kohl, 1986; Montero-Serrano et al., 2009). to the Holocene was not characterized by a gradual warming, but instead was punctuated by the cold YD interval. The Holo- PLANKTONIC FORAMINIFERAL FAUNAL DISTRIBUTION cene section of the record (1.36–0 m) is marked by a relatively very warm interval with values close to or greater than 80%. Qualitative analysis of the planktonic foraminifera allows us Particularly in the middle Holocene, the PPC values approxi- to identify 24 species lumped into 15 groups: Globigerinoides mate 95%, indicative of the Holocene Climatic Optimum (HCO). ruber alba, Globigerinoides ruber rosea, Globigerinoides sacculifer gr., Globigerina bulloides gr., Globogerinella aequi- PLANKTONIC FORAMINIFERAL ECO-BIOZONATION AND COMPARISON lateralis gr., Globorotalia scitula, Globorotalia menardii gr., WITH PREVIOUS ECO-BIOSTRATIGRAPHIC SCHEMES Orbulina universa, neogloboquadrinids, Globorotalia crassa- IN THE PERI-CARIBBEAN REGION formis, Globorotalia inflata, Globorotalia truncatulinoides, The detailed quantitative distribution of planktonic fora- Pulleniatina obliquiloculata, and Sphaeroidinella dehiscens minifera resulted in the identification of 12 eco-biozones (Fig. 2). The stratigraphic distribution of the most abundant spe- (GOMPFE 1–GOMPFE 12) spanning approximately the last cies and species groups over the last 21 kyr BP is shown in Fig- 21 kyr BP (Fig. 3). Each eco-biozone is defined by using a pro- ure 3. The overall changes in the planktonic foraminiferal abun- gressive number from the top to the base of the core and identi- dances from JPC-26 are consistent with previously docu- fied by local (re-) occurrences and/or temporary disappear- mented changes in the GoM foraminiferal assemblages related ances of the main specific taxa in association with more or less to the transition from glacial to interglacial conditions (e.g., important fluctuations of their abundance, indicative of modifi- Flower and Kennett, 1995; Poore et al., 2003). cation in marine conditions, such as vertical mixing, as well as Globigerinoides ruber, G. sacculifer gr., neogloboqua- changes in marine productivity and surface water temperature, drinids, O. universa, G. crassaformis, G. menardii gr., and salinity and/or current flow. G. truncatulinoides are the most abundant species. With the ex- ception of the representatives of G. menardii gr., that are virtu- – GOMPFE 12 (2.96–2.61 m; 21.13–20.41 ka): this is rec- ognized between the base of the succession studied and ally absent from the base of the succession up to 1.36 m, they 2.60 m. In this interval the assemblages are dominated have an almost continuous distribution throughout the interval by the cold-water species G. inflata and G. crassaformis studied. Globigerinoides ruber was the dominant species over gr. This interval is also marked by a significant contribu- the entire duration (33.2% on average). The white (G. ruber tion of O. universa to the planktonic fauna. The base of alba) and pink (G. ruber rosea) varieties of this species were this eco-biozone falls within the middle part of the counted as separate categories, showing that the white variety biozone Y2 of Kennett et al. (1985). is about 15 to 30% more abundant than the pink variety (Fig. 3). The species G. menardii gr., P. obliquiloculata, G. sacculifer gr., – GOMPFE 11 (2.61–2.36 m; 20.41–19.01 ka): this zone is bounded by two increases in G. crassaformis gr. and G. truncatulinoides display an upward increase in abun- A near-absence of G. inflata, an increase of G. ruber dance. A sporadic distribution is recorded for G. bulloides and (both varieties), the highest abundance of G. bulloides, a G. inflata, since they are significant contributors only in the strong decrease of O. universa, and the presence of basal part of the core with an average contribution of ~10–25%. G. scitula in the lower part are the main features of this The latter exists in the faunal composition up to 1.40 m and then interval. This eco-biozone corresponds to the upper part completely disappears, while the former, although it does not of the biozone Y2 of Kennett et al. (1985). disappear from the sequence, reduces its populations to <5% in the upper half of the core. Globorotalia scitula presents a dis- – GOMPFE 10 (2.36–1.91 m; 19.01–15.89 ka): the lower boundary of this eco-biozone is identified by the sudden continuous distribution and shows minor abundance peaks decrease in G. ruber rosea, an increase in G. sacculifer, and/or intervals of occurrence limited mainly to the middle part and the last consistent occurrence of G. inflata (Kennett of the core. The distribution pattern of neogloboquadrinids is et al., 1985, bioevent f8 of Antonarakou et al., 2015). It is characterized by high percentages in the upper half of the core, mainly characterized by a strong increase in abundance with their maximum percentages occurring during the deposi- (acme) of G. crassaformis gr., O. universa and G. ruber, tion of organic-rich sediments and throughout the Holocene. and the occurrence of G. truncatulinoides, neoglo- boquadrinids and G. aequilateralis which reach abun- PLANKTONIC PALAEOCLIMATIC CURVE dance values around 10%. This eco-biozone coincides with the uppermost part of the biozone Y2 of Kennett et From the base of the core up to 2.31 m (19.0 ka), the lowest al. (1985). values of the PPC (~20–40%) are indicative of the glacial pe- – GOMPFE 9 (1.91–1.79 m; 15.89–15.28 ka): this is riod (Fig. 4). This interval is characterized by the dominance of bounded by two sharp decreases in G. ruber rosea, and cold water indicators, such as G. inflata, G. crassaformis, Fig. 3. Quantitative fluctuations of planktonic foraminiferal assemblages in core JPC-26 The blue horizontal lines represent the eco-biostratigraphic boundaries, while ‘‘f” in blue symbolizes the planktonic foraminiferal bioevents recognized in core JPC-26 (Antonarakou et al., 2 0 1 5 ) ; t o t h e r i g h t i s s h o wn t h e c o r r e l a t i o n s c h e m e b e t we e n t h e p l a n k t o n i c f o r a m i n i f e r a l e c o - b i o z o n e s d e f i n e d i n t h e G o M a n d t h e c o r r e s p o n d i n g c h r o n o s t r a t i g r a p h i c f r a m e wo r k o f t h e a d j a c e n t b a s i n s ( c i r c u m - Go M / C a r i b b e a n r e g i o n ) ; OR Z – Or g a n i c - R i c h Z o n e s , R T – R e d T u r b i d i t e s , GT – Gr e e n T u r b i d i t e s Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue 183 184 Assimina Antonarakou et al. Fig. 4. Integr ated eco-biostr atigr aphic r ec or d of the JP C-26 cor e T h e s u c c e s s i o n o f 1 2 r e c o g n i z e d e c o - b i o e v e n t s i s s h o wn o n t h e l e f t ; e c o - b i o z o n e s a r e c o r r e l a t e d t o G r e e n l a n d S t a d i a l s ( i n b l u e ) a n d I n t e r s t a d i a l s ( i n r e d ) o f t h e I N T I M A T E e v e n t s t r a t i g r a p h y ( e . g . , G r e e n l a n d I c e S h e e t P r o j e c t 2 – G I S P 2 ; B l o c k l e y e t a l . , 2 0 1 2 ) a n d t o t h e M a n g e r u d e t a l . ( 1 9 7 4 ) c l i m a t i c e v e n t s ; t h e a g e s o b t a i n e d f o r e c o - b i o z o n e b o u n d a r i e s a r e a l s o s h o wn ; c l i m a t i c e v e n t s a r e further highlighted by the G. ruber relative abundance fluctuations during the last deglaciation, the planktonic palaeoclimatic curve (PPC), and by the morphotype-specific (G. ruber s.l.) d18O, and M g / C a r e c o r d s o f t h e c o r e s t u d i e d ( A n t o n a r a k o u e t a l . , 2 0 1 5 ) ; o t h e r e xp l a n a t i o n a s i n F i g u r e 3 Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue 185 is further characterized by strong turnover in abundance G. sacculifer and O. universa are well-represented. The between the white and pink varieties of G. ruber. The as- re-appearance of G. crassaformis (bioevent f3 of Anto- semblages are characterized by an increase of narakou et al., 2015) and decreases in G. bulloides, G. bulloides, and the significant presence of warm water G. sacculifer gr., and G. aequilateralis gr. are also indic- species (e.g., G. sacculifer gr., O. universa, G. aequi- ative of this interval. This eco-biozone is congruent with lateralis gr.), indicative of the beginning of deglaciation. the middle part of biozone Z1 of Kennett et al. (1985). This eco-biozone matches the lowermost part of – GOMPFE 1 (0.36–0 m; 2.38–0.51 ka): this is present in biozone Y1 of Kennett et al. (1985). the uppermost part of the record. It is characterized by a – GOMPFE 8 (1.79–1.65 m; 15.28–13.77 ka): this interval strong increase in P. oblioquiloculata, O. universa and is marked by a progressive upwards decrease in G. menardii gr. Near to the top of this eco-biozone, the G. crassaformis gr., the re-occurrence of G. scitula, the minimum and maximum abundances of G. ruber and near-disappearance of G. inflata, and a concomitant in- P. oblioquiloculata (bioevents f1–f2 of Antonarakou et crease in neogloboquadrinids. In the upper part a signifi- al., 2015; Poore et al., 2003) are recognized. All these cant peak of G. bulloides marks the top of this concomitant bioevents together with the completely ab- eco-biozone. This eco-biozone coincides with the mid- sence of G. bulloides and S. dehiscens represent a dis- dle part of the biozone Y1 of Kennett et al. (1985). tinctive late Holocene feature in the GoM. This – GOMPFE 7 (1.65–1.53 m; 13.77–13.09 ka): the compo- eco-biozone corresponds to the uppermost part of sition of this planktonic microfauna is similar to that of biozone Z1 of Kennett et al. (1985). eco-biozone 8, but differs by the absence of G. bulloides and G. scitula, and the last occurrence of G. inflata. At the base of this eco-biozone, P. oblioquiloculata appears DISCUSSION in the assemblages. This eco-biozone can be related with the middle part of biozone Y1 of Kennett et al. ECO-BIOSTRATIGRAPHIC APPROACH (1985). IN SUBTROPICAL MARGINAL SETTINGS – GOMPFE 6 (1.53–1.36 m; 13.09–11.70 ka): this eco-biozone shows a microfaunal composition drasti- The quantitative distribution of planktonic foraminifera from cally different to that of the previous zone, suggesting the LGM to the present displays a succession of microfaunal that it corresponds to the YD. Re-occurrences of G. sci- assemblages (biozones) characterizing the progressively tula and G. bulloides define its base. In the intermediate changing surface water environment. In such marginal basins, interval, the assemblages are characterized by an in- the successive faunal zones can be indicated as ecozones, be- crease in G. crassaformis, a decrease in O. universa cause the majority of the species are sensitive indicators of past and the presence of G. truncatulinoides and environmental changes with amplified signals (Drinia and neogloboquadrinids. This eco-biozone is equivalent to Antonarakou, 2003; Antonarakou et al., 2007, 2018, 2019; the top of the biozone Y1 of Kennett et al. (1985). Drinia et al., 2007, 2008, 2016; Kontakiotis, 2012, 2016; – GOMPFE 5 (1.36–1.26 m; 11.70–10.20 ka): high abun- Kontakiotis et al., 2013, 2016a, b, 2017; Fenton et al., 2016; dances of G. sacculifer gr. and neogloboquadrinids, a Karakitsios et al., 2017a, b). The ecological divergence be- gradual decrease in G. ruber alba and the absence of tween the species (Hemleben et al., 1989; Rohling et al., 1993), G. scitula and G. inflata characterize eco-biozone 5, the even between different morphotypes of the same species base of which is marked by the first consistent appear- (Antonarakou et al., 2015; Kontakiotis et al., 2017), determined ance of G. menardii group ( bioevent f7 of Antonarakou by different controlling factors (e.g., depth habitats, growth opti- et al., 2015). This eco-biozone corresponds to biozone mum/stressed conditions, productivity, stratification, near-/off- Y1A of Kennett et al. (1985). shore-conditions), in combination with their different test mor- – GOMPFE 4 (1.26–1.01 m; 10.20–6.83 ka): this phologies (e.g., related to shell shape and size, thickness, inner eco-biozone is defined by a re-increase in G. ruber alba, porosity and pore surface distribution; Morard et al., 2009; G. sacculifer gr. and neogloboquadrinids, as well as the Kontakiotis et al., 2017), control directly their distribution pattern presence of G. scitula. The base is defined by the peak and reflect the regional climate variability (Marcott et al., 2013). of G. sacculifer gr. (Poore et al., 2003) and minimum Therefore, this study uses the concept of “assemblage abundance of G. ruber alba (bioevent f6 of Antonarakou eco-biozones” to refer to the ecological response of planktonic et al., 2015), while the top is marked by the disappear- foraminifera to environmental changes, rather than evolution- ance of G. crassaformis, which is indicative of the ary changes. In this sense planktonic foraminifera are important mid-Holocene Z1/Z2 boundary (Kennett et al., 1985; palaeocological and palaeoclimatological indicators and such bioevent f5 of Antonarakou et al., 2015) in the GoM. This subdivision of their record provides significant insights into the eco-biozone coincides with biozone Z2 of Kennett et al. hydrological dynamics of the basin studied. Moreover, the ap- (1985). plied eco-biostratigraphic scheme effectively reflects the global – GOMPFE 3 (1.01–0.71 m; 6.83–5.16 ka): a great expan- climatic oscillations during the latest Quaternary. The applica- sion of warm water species characterizes eco-biozone bility of this approach has been tested in many sediment cores 3. The base of this interval is marked by the first consis- collected in various marginal basins (e.g., Aegean Sea, Ionian tent occurrence of S. dehiscens. Increasing percentages Sea, Adriatic Sea, Tyrrhenian Sea, Caribbean Sea). The con- of warm water species (G. ruber alba, G. sacculifer gr.; struction of such a detailed eco-biochronostratigraphic frame- bioevent f4 of Antonarakou et al., 2015) and a strong re- work through the identification of these bio-ecoevents in other duction or absence of neogloboquadrinids and G. scitula more or less distant cores permits the refinement of previous characterize this eco-biozone that represents the lower Late Quaternary regional schemes (Ericson and Wollin, 1968; part of biozone Z1 of Kennett et al. (1985). Ruddiman, 1971; Kennett and Huddlestun, 1972; Kennett et al., – GOMPFE 2 (0.71–0.36 m; 5.16–2.38 ka): this is mainly 1985; Flower and Kennett, 1990; Martin et al., 1990; Wilson, characterized by an abrupt increase in G. menardii gr., 2012), makes a precise correlation between them and facili- while other warm water species such as G. ruber, tates palaeoclimatic and/or palaeoceanographic interpretations 186 Assimina Antonarakou et al. of the time interval studied. Any minor discrepancies between G. bulloides, G. ruber and O. universa). Mg/Ca-based esti- the present and previous studies concern the degree of mates show a relatively stable climate period with SSTs around synchroneity between the bio-ecozone boundaries, being due 22°C. However, in the middle part of this eco-biozone to (1) the different size fractions in planktonic foraminifera anal- (~17.0 ka), which has been ascribed to the Heinrich 1 event yses adopted by the authors (>100, 125, 150 or 175 µm), (2) (Antonarakou et al., 2015), an intensification of cold conditions dating uncertainties of 14C ages probably due to the application is suggested by the occurrence of the heaviest d18O values in of a constant sea-surface 14C reservoir age correction in previ- the whole record. Eco-biozone GOMPFE 9 corresponds to the ous studies, especially during the late glacial–interglacial transi- upper part of GS2a. The strong negative excursion in PPC and tion (e.g., Broecker et al., 1988), and to (3) an absence or a Mg/Ca-SST records at the base of this interval may be tenta- weak accuracy of 14C dating performed in some cases, on tively related to the Oldest Dryas (OD) event, the age of which in mixed benthic foraminifera and on pteropods (e.g., Kennett et the GoM is documented between 16.0 and 14.7 ka (Lea et al., al., 1985; Flower and Kennett, 1990). 2003; Williams et al., 2010). The GOMPFE9/8 boundary is close to the boundary be- LATE PLEISTOCENE–HOLOCENE INTEGRATED tween the GS-2a and GI-1 events. In this interval, a tendency CHRONOSTRATIGRAPHIC FRAMEWORK, PALAEOCEANOGRAPHIC toward warmer conditions is indicated by an upwards decreas- EVENT STRATIGRAPHY AND PALAEOENVIRONMENTAL IMPLICATIONS ing trend of cold water species (e.g., G. crassaformis) abun- dances and by a relative warming trend inferred from significant A planktonic foraminiferal eco-biostratigraphy was com- d18O depletion in the isotopic record and concomitant increased bined with the palaeoclimatic JPC-26 records to obtain a de- temperatures in the Mg/Ca-based record. Eco-biozones 8 and tailed late Pleistocene–Holocene integrated stratigraphic 7 correspond to the interstadial BÝlling/AllerÝd (B/A) sensu framework for the GoM (Fig. 4). Short-term climatic and faunal Mangerud et al. (1974) and the Greenland GI-1 episode (Lowe fluctuations recognized during this time span can be compared et al., 2008) dated to between 14.8 and 13.0 ka. This event falls to those proposed by the INTIMATE group (Björck et al., 1998; within the organic-rich deposits ORZ II–III, where a strong Lowe et al., 2008; Blockley et al., 2012) in Greenland ice cores. change in sedimentation rate and in planktonic biodiversity is In the lowermost part of the succession studied, eco-bio- recorded. These features prevent the identification of high-res- zones GOMPFE 12 and GOMPFE 11 cover the time interval be- olution climate oscillations. The observed climatic oscillations tween 21.1 and 19.0 ka, which chronologically corresponds to during the GI-1 event show three warm/humid – GI-1e (BÝlling ) the GS-2b event of the late glacial period and includes the LGM. and GI-1a,c (AllerÝd) – events that were interrupted by two During this interval, the planktonic assemblages show generally cold/dry – GI-1d (Older Dryas ) and GI-1b (Intra AllerÝd Cold low diversity and are dominated by species indicating cold and Period; IACP) events on a centennial scale. All these short-term productive water conditions. The coldest interval is identified in oscillations are considered to be contemporaneous with GI-1e all climatic records (d18O, Mg/Ca-SSTs, PPC) at the top of to GI-1a of the ice-core record (Fig. 4), suggesting a climatic link eco-biozone GOMPFE 12, characterized by a significant de- between the study area and the high-latitude areas. crease in the warm water species G. ruber rosea and by the Overall, an important climatic warming (5–7°C based on highest abundances of G. inflata and G. crassaformis, indicative Mg/Ca-SSTs in GI-1e; Antonarakou et al., 2015) and the pres- of rather cool and deep mixed layers. In this part, heavier d18O ence of warm and seasonally stratified water masses are in- values and minimum SSTs of about 19°C are also recorded and ferred from the structure of the assemblages of these associated with the LGM (Antonarakou et al., 2015). Neverthe- eco-biozones, characterized by the presence of G. truncatu- less during the LGM, GoM SSTs do not display continuously low linoides and neogloboquadrinids. The d18O record, on the temperature values, which is consistent with relevant climate re- whole, shows a tendency to lighter values, suggesting a climatic cords from the tropical and subtropical Atlantic (Bard et al., 2000; amelioration. However, the upwards deglaciation trend is often Flower et al., 2004; Schmidt et al., 2004; Weldeab et al., 2006). A interrupted by brief cooling events, expressed by positive iso- noticeable event, that could partly explain this slight SST rise, is tope excursions and/or SST negative peaks. Such an abrupt the sudden increase of G. ruber alba, as suggested by clear pos- Mg/Ca-SST cold spell (~3°C), concomitant with a slight de- itive fluctuations (e.g., in the upper part of eco-biozone crease in PPC and d18O records, characterizes the uppermost GOMPFE 11). Generally, G. ruber fluctuations have been con- part of eco-biozone 8, attributed to the stadial GI-1d event dated sidered good recorders of climate variability (Sprovieri et al., in our record to ~13.8 ka. A decrease in G. ruber and 2006a, 2012; Budillon et al., 2009; Antonarakou et al., 2015), O. universa accompanied by an increase of neogloboqua- with its relative abundance positively co-varying with SST drinids defines the planktonic foraminiferal assemblage. A no- (Hagen and Keigwin, 2002; Sprovieri et al., 2006b) and its abun- ticeable event is the temporary absence of G. scitula in this time dance oscillations strongly controlled by global climate forcing interval, which records the zonal boundary between GI-1d and (Sprovieri et al., 2006b). Despite the predominance of cold spe- GI-1c (Minisini et al., 2007; Rouis-Zargouni et al., 2010; Siani et cies during the glacial period, an increase (27.8–51.2%) of al., 2010). G. ruber alba during the LGM is a common feature of marginal The following eco-biozone GOMPFE 7 covers the time in- records (circum-GoM/Caribbean region, Mediterranean Sea), terval between 13.7 and 13.0 ka and is attributed to the probably due to the fact that during the LGM SSTs do not display interstadial GI-1c event as indicated by SST reconstruction. their lowest values (Cacho et al., 2001; Sbaffi et al., 2004; Siani This interpretation fits well with the planktonic foraminiferal con- et al., 2010; Kontakiotis, 2016). tent, characterized by a progressive increase in warm water Eco-biozone GOMPFE 10 corresponds to the GS-2a clima- taxa (G. ruber, G. sacculifer gr., O. universa). The beginning of tic event and includes the first step of the last deglaciation, this event is punctuated by the re-occurrence of O. universa in- dated in the subtropical Atlantic to between 19.0 and 12.6 ka dicating in combination with G. ruber the establishment of a (Aharon, 2003, 2006; Carlson et al., 2008; Sionneau et al., seasonal thermocline (Tedesco and Thunell, 2003; Tedesco et 2010; Schmidt and Lynch-Stieglitz, 2011; Antonarakou et al., al., 2007; Wejnert et al., 2010). The d18O signal indicates a 2015). A slight decrease in the planktonic foraminiferal diversity strong depletion at the base (GI-1c), and a weak upwards en- characterizes the assemblage, dominated by both warm and richment trend to cooler sea surface water conditions, which is cold water species (G. crassaformis, neogloboquadrinids, attributed to the IACP/GI-1b event (Alley et al., 1993). Finally, at Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue 187 the top of this interval, a significant warming of about 3.5°C and progressively through the following eco-biozone, the d18O (GI-1a) is marked in the Mg/Ca-SST record. However, this record shows the onset upwards of strong enrichment and de- event is not recorded in the PPC and d18O records, most likely pletion phases corresponding to a long period of marked sea- due to the lower resolution of the sedimentary record and/or sonality throughout the late Holocene, possibly associated with bioturbation effects in this part of the succession. relative changes in Mississippi River runoff. Finally, eco-biozone Following this warm interval, both Mg/Ca and d18O records GOMPFE 1 presents the typical modern foraminiferal associa- show a cooling trend of 3.5°C centered on 12.9–12.7 ka, proba- tion, dominated by temperate and subtropical taxa (Dowsett et bly representing the strong climatic cooling linked to the GS-1 al., 2003; Richey et al., 2007; Poore et al., 2013; Arellano-Torres event in the Greenland ice core records and the GS-1 period, and Machain-Castillo, 2017). dated in core JPC-26 between 13.0 and 12.5 ka. The features of the assemblages (significant increase in cold water eutrophic species associated with a decrease in warm water taxa) indi- CONCLUSIONS cate a glacial period of generally high surface water fertility that characterizes this eco-biozone (GOMPFE 6). The multidisciplinary approach used here results in a de- The Holocene section of the record corresponds to tailed chronostratigraphic framework for the last 21 ka for the eco-biozones GOMPFE 1–5, and is marked by higher diversity in GoM (also valid for the peri-Caribbean region), based on the planktonic assemblages compared to the previous eco- study of associations of planktonic foraminifera from the biozones, and a relatively warm interval [negative d18O values, deep-sea and the high sedimentation rate core JPC-26. Twelve elevated Mg/Ca and PPC values; (–0.71)–(–3.42‰), ~24–30°C eco-biozones (GOMPFE 1–12) were identified by sharp and >70% respectively], but with pronounced warm-cold oscilla- changes in planktonic foraminiferal taxa and compared to the tions with well-defined minima (e.g., at 6.1, 5.6, and 1.1 ka). The stratigraphic event scheme proposed by the INTIMATE group latest Holocene delimits eco-biozone 5, which spans a short time in order to better identify the relationships between past climatic interval (11.7–10.2 ka) in the JPC-26 record. SSTs reached Ho- changes and the response of microfaunal assemblages in the locene values with a mean amplitude change observed during subtropical Atlantic. Most of these downcore faunal variations in the YD/Holocene transition of about 2°C. However, the climatic relation to SST oscillations represent millennial to centennial amelioration is more evident in the following eco-biozone climatic variability, which are recorded in Greenland ice cores (GOMPFE 4), corresponding to the HCO interval, where lighter over the last deglaciation. Among them, we recognized the gla- d18O and higher PPC values are recorded. The latter also in- cial GS-2a to GS-2b events, the interstadial B-A/GI-1a-d cludes eco-biozone GOMPFE 3, and is the result of a substantial events, the YD/GS-1 and the Holocene warm interval. More- increase in warm water taxa (G. ruber, O. universa, G. sacculifer over, the recognition of a stratigraphic relationship between gr., and G. aequilateralis gr.) and the progressive reduction (into planktonic foraminiferal bioevents and organic-rich sediments GOMPFE 4) or absence (into GOMPFE 3) of G. crassaformis enhances the possibility for reliably correlating marine records and G. scitula. The occurrence of a short cooling event in the in such marginal settings, offering a better comprehension of lower part of eco-biozone 3 (~6.1 ka) is suggested by significant the palaeoceanographic history of these basins. These findings d18O depletion and reduction in the Globigerinoides ruber per- represent a refinement and extension of previous eco-bio- centages, coupled with an increase in abundances of Globo- stratigraphic records in the subtropical Atlantic, facilitating re- rotalia truncatulinoides as well as the re-occurrence of gional and widespread climatic and microfaunal correlations Globigerina bulloides. All these features in the planktonic assem- over the last 21 ky. A conclusive correlation of this work with blages represent an episode of improved ventilation in this basin others well known from close or more distal areas indicated the attesting to deep winter convection and vertical mixing in the wa- robustness of these results, with particular emphasis on ter column (Schmuker and Schiebel, 2002; Arellano-Torres and multi-disciplinary strategies and multiproxy studies performed Machain-Castillo, 2017). This may correlate with the global-scale on late Quaternary cores with high sedimentation rates, which rapid climate change (RCC) at 6.0–5.0 ka BP reported in the can provide a powerful tool for monitoring the palaeoclimatic Middle Holocene by Mayewski et al. (2004). A subsequent SST evolution of the subtropical Atlantic in relation to the global cli- rise between 5.1–2.4 ka delineates ecobiozone GOMPFE 2. The matic system over the last glacial cycle. PPC signal is close enough to its maximum values, and the spe- cies G. ruber, G. sacculifer, G. menardii gr. and neogloboqua- Acknowledgements. Constructive comments by two drinids are the main constituents of the planktonic fauna. The anonymous reviewers were critical to improving this manu- near-absence of G. crassaformis, G. inflata and G. scitula may script, and Dr. W. Granoszewski (Co-Editor) is also thanked for indicate that reduced oxygenation in the deeper water column his editorial handling. was detrimental to that species, suggesting stable stratification and poor deep-water ventilation in the GoM. Within this interval REFERENCES Aharon, P., 2003. Meltwater flooding events in the Gulf of Mexico re- Alley, R.B., Meese, D.A., Shuman, C.A., Gow, A.J., Taylor, K.C., visited: implications for rapid climate changes during the last Grootes, P.M., White, J.W.C., Ram, M., Waddington, E.D., deglaciation. Paleoceanography, 18: 1079 doi:10.1029/2002PA Mayewski, P.A., Zielinski, G.A., 1993. Abrupt increase in 000840. Greenland snow accumulation at the end of the Younger Dryas Aharon, P., 2006. Entrainment of meltwaters in hyperpycnal flows event. Nature, 362: 527. during deglaciation superfloods in the Gulf of Mexico. Earth and Antonarakou, A., Drinia, H., Tsaparas, N., Dermitzakis, M.D., Planetary Science Letters, 241: 260–270. 2007. Micropaleontological parameters as proxies of Late Mio- 188 Assimina Antonarakou et al. cene surface water properties and paleoclimate in Gavdos Is- ages obtained on coexisting planktonic foraminifera. Paleo- land, Eastern Mediterranean. Geodiversitas, 29: 379–399. ceanography, 3: 647–657. Antonarakou, A., Kontakiotis, G., Mortyn, P.G., Drinia, H., Budillon, F., Lirer, F., Iorio, M., MacrÒ, P., Sagnotti, L., Vallefuoco, Sprovieri, M., Besiou, E., Tripsanas, E., 2015. Biotic and geo- M., Ferraro, L., Garziglia, S., Innangi, S., Sahabi, M., Tonielli, chemical (d18O, d13C, Mg/Ca, Ba/Ca) responses of R., 2009. Integrated stratigraphic reconstruction for the last 80 Globigerinoides ruber morphotypes to upper water column vari- kyr in a deep sector of the Sardinia Channel (Western Mediterra- ations during the last deglaciation, Gulf of Mexico. Geochimica nean). Deep Sea Research Part II: Topical Studies in Oceanog- et Cosmochimica Acta, 170: 69–93. raphy, 56: 725–737. Antonarakou, A., Kontakiotis, G., Zarkogiannis, S., Mortyn, Cacho, I., Grimalt, J.O., Canals, M., Sbaffi, L., Shackleton, N.J., P.G., Drinia, H., Koskeridou, E., Anastasakis, G., 2018. Schönfeld, J., Zahn, R., 2001. Variability of the western Medi- Planktonic foraminiferal abnormalities in coastal and open ma- terranean Sea surface temperature during the last 25,000 years rine eastern Mediterranean environments: a natural stress mon- and its connection with the Northern Hemisphere climatic itoring approach in recent and early Holocene marine systems. changes. Paleoceanography, 16: 40–52. Journal of Marine Systems, 181: 63–78. Capotondi, L., Maria Borsetti, A., Morigi, C., 1999. Foraminiferal Antonarakou, A., Kontakiotis, G., Vasilatos, C., Besiou, E., ecozones, a high resolution proxy for the late Quaternary Zarkogiannis, S., Drinia, H., Mortyn, P.G., Tsaparas, N., biochronology in the central Mediterranean Sea. Marine Geol- Makri, P., Karakitsios, V., 2019. Evaluating the effect of marine ogy, 153: 253–274. diagenesis on Late Miocene pre-evaporitic sedimentary suc- Carlson, A.E., Oppo, D.W., Came, R.E., LeGrande, A.N., cessions of eastern Mediterranean Sea. IOP Conference Se- Keigwin, L.D., Curry, W.B., 2008. Subtropical Atlantic salinity ries: Earth and Environmental Sciences, 221: 012051 doi: variability and Atlantic meridional circulation during the last 10.1088/1755-1315/221/1/012051. deglaciation. Geology, 36: 991–994. Antonov, J.I., Seidov, D., Boyer, T.P., Locarnini, R.A., Mishonov, Caromel, A.G.M., Schmidt, D.N., Phillips, J.C., Rayfield, E.J., A.V., Garcia, H.E., Baranova, O.K., Zweng, M.M., Johnson, 2014. Hydrodynamic constraints on the evolution and ecology of D.R., 2010. World Ocean Atlas 2009, Volume 2: Salinity. In: planktic foraminifera. Marine Micropaleontology, 106: 69–78. NOAA Atlas NESDIS 69 (ed. S. Levitus). Washington, D.C., Chen, S., Hu, C., 2017. Estimating sea surface salinity in the north- U.S. Gov. Printing Office. ern Gulf of Mexico from satellite ocean color measurements. Arellano-Torres, E., Machain-Castillo, M.L., 2017. Late Pleisto- Remote Sensing of Environment, 201: 115–132. cene–Holocene variability in the southern Gulf of Mexico sur- Corbett, D.R., McKee, B., Duncan, D., 2004. An evaluation of mo- face waters based on planktonic foraminiferal assemblages. bile mud dynamics in the Mississippi River deltaic region. Ma- Marine Micropaleontology, 131: 44–58. rine Geology, 209: 91–112. Auladell, M., Pelegrí, J.L., García-Olivares, A., Kirwan, A.D., Del Monte-Luna, P., Villalobos, H., Arreguín-Sánchez, F., 2015. Lipphardt, B.L., Martín, J.M., Pascual, A., Sangr´, P., Zweng, Variability of sea surface temperature in the southwestern Gulf M., 2010. Modelling the early evolution of a Loop Current ring. of Mexico. Continental Shelf Research, 102(C): 73–79. Journal of Marine Systems, 80: 160–171. Dowsett, H.J., Verardo, S., Poore, R.Z., 2003. Gulf of Mexico Bard, E., Rostek, F., Turon, J.-L., Gendreau, S., 2000. Hydrologi- planktonic foraminifer transfer function GOM2: preliminary re- cal Impact of Heinrich Events in the Subtropical Northeast At- port. U.S. Geological Survey Open-File Report OF 03-61. lantic. Science, 289: 1321–1324. Drinia, H., Antonarakou, A., 2003. Late Miocene paleoclimatic Behringer, D.W., Molinari, R.L., Festa, J.F., 1977. The variability of variations in the Eastern Mediterranean: an ecostratigraphical anticyclonic current patterns in the Gulf of Mexico. Journal of approach. Neues Jahrbuch für geologie und Paläontologie, 10: Geophysical Research, 82: 5469–5476. 603–616. Biggs, D.C., Müller-Karger, F.E., 1994. Ship and satellite observa- Drinia, H., Antonarakou, A., Tsaparas, N., Kontakiotis, G., 2007. tions of chlorophyll stocks in interacting cyclone-anticyclone Palaeoenvironmental conditions preceding the Messinian Salin- eddy pairs in the western Gulf of Mexico. Journal of Geophysical ity Crisis: A case study from Gavdos Island. Geobios, 40: Research: Oceans, 99: 7371–7384. 251–265. Björck, S., Walker, M.J.C., Cwynar, L.C., Johnsen, S., Ka- Drinia, H., Antonarakou, A., Kontakiotis, G., 2008. On the occur- ren-Luise, K., Lowe, J.J., Wohlfarth, B., 1998. An event stra- rence of Early Pliocene marine deposits in Ierapetra basin, E. tigraphy for the Last Termination in the North Atlantic region Crete. Bulletin of Geosciences, 83: 63–78. based on the Greenland ice-core record: a proposal by the Drinia, H., Antonarakou, A., Tsourou, T., Kontakiotis, G., INTIMATE group. Journal of Quaternary Science, 13: 283–292. Psychogiou, M., Anastasakis, G., 2016. Foraminifera Blockley, S.P.E., Lane, C.S., Hardiman, M., Rasmussen, S.O., eco-biostratigraphy of the southern Evoikos outer shelf, central Seierstad, I.K., Steffensen, J.P., Svensson, A., Lotter, A.F., Aegean Sea, during MIS 5 to present. Continental Shelf Re- Turney, C.S.M., Bronk Ramsey, C., 2012. Synchronisation of search, 126: 36–49. palaeoenvironmental records over the last 60,000 years, and an Elliott, B.A., 1982. Anticyclonic Rings in the Gulf of Mexico. Journal extended INTIMATE event stratigraphy to 48,000 b2k. Quater- of Physical Oceanography, 12: 1292–1309. nary Science Reviews, 36: 2–10. Ericson, D.B., Wollin, G., 1968. Pleistocene Climates and Chronol- Blumberg, A.F., Mellor, G.L., 1985. A simulation of the circulation in ogy in Deep-Sea Sediments. Science, 162: 1227–1234. the Gulf of Mexico. Israel Journal of Earth Sciences, 34: Fenton, I.S., Pearson, P.N., Dunkley Jones, T., Purvis, A., 2016. 122–144. Environmental Predictors of Diversity in Recent Planktonic Bonfardeci, A., Caruso, A., Bartolini, A., Bassinot, F., Foraminifera as Recorded in Marine Sediments. PLOS ONE, Blanc-Valleron, M.-M., 2018. Distribution and ecology of the 11: e0165522. Globigerinoides ruber–Globigerinoides elongatus morphotypes Flower, B.P., Kennett, J.P., 1990. The Younger Dryas Cool Episode in the Azores region during the late Pleistocene–Holocene. in the Gulf of Mexico. Paleoceanography, 5: 949–961. Palaeogeography, Palaeoclimatology, Palaeoecology, 491: Flower, B.P., Kennett, J.P., 1995. Biotic responses to temperature 92–111. and salinity changes during the last deglaciation, Gulf of Mexico. Bouma, A.H., Stelting, C.E., Coleman, J.M., 1985. Mississippi In: Commission on Geosciences, Effects of Past Global Fan, Gulf of Mexico. In: Submarine Fans and Related Turbidite Changes on Life: 209–220. National Academy Press, Washing- Systems(eds. A.H. Bouma, W.R. Normark and N.E. Barnes): ton, D.C. 143–150. Springer New York, New York. Flower, B.P., Hastings, D.W., Hill, H.W., Quinn, T.M., 2004. Phas- Broecker, W.S., 1991. The great ocean conveyor. Oceanography, ing of deglacial warming and Laurentide Ice Sheet meltwater in 4: 79–89. the Gulf of Mexico. Geology, 32: 597–600. Broecker, W.S., Andree, M., Bonani, G., Wolfli, W., Klas, M., Mix, Gopalakrishnan, G., Cornuelle, B.D., Hoteit, I., Rudnick, D.L., A., Oeschger, H., 1988. Comparison between radiocarbon Owens, W.B., 2013. State estimates and forecasts of the loop Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue 189 current in the Gulf of Mexico using the MITgcm and its adjoint. Kontakiotis, G., Antonarakou, A., Mortyn, P.G., Drinia, H., Journal of Geophysical Research: Oceans, 118: 3292–3314. Anastasakis, G., Zarkogiannis, S., Möbius, J., 2017. Morpho- Hagen, S., Keigwin, L.D., 2002. Sea-surface temperature variabil- logical recognition of Globigerinoides ruber morphotypes and ity and deep water reorganisation in the subtropical North Atlan- their susceptibility to diagenetic alteration in the eastern Medi- tic during Isotope Stage 2–4. Marine Geology, 189: 145–162. terranean Sea. Journal of Marine Systems, 174: 12–24. Hemleben, C., Spindler, M., Anderson, O.R., 1989. Modern Plank- Koutrouli, A., Anastasakis, G., Kontakiotis, G., Ballengee, S., tonic Foraminifera. Springer, New York. Kuehn, S., Pe-Piper, G., Piper, D.J.W., 2018. The early to Hofmann, E.E., Worley, S.J., 1986. An investigation of the circula- mid-Holocene marine tephrostratigraphic record in the Nisyros- tion of the Gulf of Mexico. Journal of Geophysical Research: Yali-Kos volcanic center, SE Aegean Sea. Journal of Volcanol- Oceans, 91: 14221–14236. ogy and Geothermal Research, 366: 96–111. INEGI, 2014. Anuario Estadístico y Geográfico por Entidad Federativa Lea, D.W., Pak, D.K., Peterson, L.C., Hughen, K.A., 2003. Syn- (in Spain). Instituto Nacional de Estadística y Geografía, Mexico. chroneity of Tropical and High-Latitude Atlantic Temperatures Jochens, A.E., DiMarco, S.F., 2008. Physical oceanographic con- over the Last Glacial Termination. Science, 301: 1361–1364. ditions in the deepwater Gulf of Mexico in summer 2000–2002. Leventer, A., Williams, D.F., Kennett, J.P., 1983. Relationships be- Deep Sea Research Part II: Topical Studies in Oceanography, tween anoxia, glacial meltwater and microfossil preservation in 55: 2541–2554. the Orca Basin, Gulf of Mexico. Marine Geology, 53: 23–40. Jonkers, L., Reynolds, E., Richey, J., Hall, I.R., 2015. Lunar peri- Limoges, A., de Vernal, A., Van Nieuwenhove, N., 2014. odicity in the shell flux of planktonic foraminifera in the Gulf of Long-term hydrological changes in the northeastern Gulf of Mexico. Biogeosciences, 12: 3061–3070. Mexico (ODP-625B) during the Holocene and late Pleistocene Karakitsios, V., Roveri, M., Lugli, S., Manzi, V., Gennari, G., inferred from organic-walled dinoflagellate cysts. Palaeoge- Antonarakou, A., Triantaphyllou, M., Agiadi, K., Kontakiotis, ography, Palaeoclimatology, Palaeoecology, 414: 178–191. G., Kafousia, N., de Rafelis, M., 2017a. A record of the Liu, Y., Lee, S.-K., Muhling, B.A., Lamkin, J.T., Enfield, D.B., Messinian salinity crisis in the eastern Ionian tectonically active 2012. Significant reduction of the Loop Current in the 21st cen- domain (Greece, eastern Mediterranean). Basin Research, 29: tury and its impact on the Gulf of Mexico, Journal of Geophysical 203–233. Research, 117, C05039-8, doi: 10.1029/2011JC007555 Karakitsios, V., Cornée, J.-J., Tsourou, T., Moissette, P., Konta- Locarnini, R.A., Mishonov, A.V., Antonov, J.I., Boyer, T.P., Gar- kiotis, G., Agiadi, K., Manoutsoglou, E., Triantaphyllou, M., cia, H.E., Baranova, O.K., Zweng, M.M., Johnson, D.R., 2010. Koskeridou, E., Drinia, H., Roussos, D., 2017b. Messinian sa- World Ocean Atlas 2009, Volume 1: Temperature. In: NOAA At- linity crisis record under strong freshwater input in marginal, in- las NESDIS 68 (ed. S. Levitus). U.S. Government Printing Of- termediate, and deep environments: the case of the North fice, Washington, D.C. Aegean. Palaeogeography Palaeoclimatology Palaeoecology, LoDico, J.M., Flower, B.P., Quinn, T.M., 2006. Subcen- 485: 316–335. tennial-scale climatic and hydrologic variability in the Gulf of Kennett, J.P., Huddlestun, P., 1972. Late Pleistocene paleoclima- Mexico during the early Holocene. Paleoceanography, 21: tology, foraminiferal biostratigraphy and tephrochronology, PA3015, doi: 10.1029/2005PA001243 western Gulf of Mexico. Quaternary Research, 2: 38–69. Lowe, J.J., Rasmussen, S.O., Björck, S., Hoek, W.Z., Kennett, J.P., Srinivasan, M.S., 1983. Neogene Planktonic Fora- Steffensen, J.P., Walker, M.J.C., Yu, Z.C., 2008. minifera: a Phylogenetic Atlas. Hutchinson Ross Publishing Synchronisation of palaeoenvironmental events in the North At- Company, New York. lantic region during the Last Termination: a revised protocol rec- Kennett, J.P., Elmstrom, K., Penrose, N., 1985. The last ommended by the INTIMATE group. Quaternary Science Re- deglaciation in orca basin, gulf of Mexico: high-resolution plank- views, 27: 6–17. tonic foraminiferal changes. Palaeogeography, Palaeoclimato- Luo, H., Bracco, A., Cardona, Y., McWilliams, J.C., 2016. logy, Palaeoecology, 50: 189–216. Submesoscale circulation in the northern Gulf of Mexico: Sur- Kontakiotis, G., 2012. Palaeoceanographic and palaeoclimatic face processes and the impact of the freshwater river input. study of Eastern Mediterranean during Late Quaternary, based Ocean Modelling, 101: 68–82. on planktonic foraminiferal assemblages (in Greek with English Mangerud, J.A.N., Andersen, S.T., Berglund, B.E., Donner, J.J., extended abstract). National and Kapodistrian University of Ath- 1974. Quaternary stratigraphy of Norden, a proposal for termi- ens, Athens, Greece. nology and classification. Boreas, 3: 109–126. Kontakiotis, G., 2016. Late Quaternary paleoenvironmental recon- Marcott, S.A., Shakun, J.D., Clark, P.U., Mix, A.C., 2013. A Recon- struction and paleoclimatic implications of the Aegean Sea struction of Regional and Global Temperature for the Past (eastern Mediterranean) based on paleoceanographic indexes 11,300 Years. Science, 339(6124): 1198–1201. and stable isotopes. Quaternary International, 401: 28–42. Marino, G., Rohling, E.J., Sangiorgi, F., Hayes, A., Casford, J.L., Kontakiotis, G., Mortyn, P.G., Antonarakou, A., Martínez-Botí, Lotter, A.F., Kuèera, M., Brinkhuis, H., 2009. Early and middle M.ƒ., Triantaphyllou, M.V., 2011. Field-based validation of a Holocene in the Aegean Sea: interplay between high and low diagenetic effect on G. ruber Mg/Ca paleothermometry: core top latitude climate variability. Quaternary Science Reviews, 28: results from the Aegean Sea (eastern Mediterranean). Geo- 3246–3262. chemistry Geophysics Geosystems, 12: Q09004 doi: Martin, R.E., Johnson, G.W., Neff, E.D., Krantz, D.W., 1990. Qua- 10.1029/2011GC003692 ternary planktonic foraminiferal assemblage zones of the north- Kontakiotis, G., Antonarakou, A., Zachariasse, W.J., 2013. Late east Gulf of Mexico, Colombia Basin (Caribbean Sea), and trop- Quaternary palaeoenvironmental changes in the Aegean Sea: ical Atlantic Ocean: Graphic correlation of microfossil and oxy- interrelations and interactions between north and south Aegean gen isotope datums. Paleoceanography, 5: 531–555. Sea. Bulletin of the Geological Society of Greece, 47: 167–177. Mayewski, P.A., Rohling, E.E., Curt Stager, J., Karlén, W., Kontakiotis, G., Karakitsios, V., Mortyn, P.G., Antonarakou, A., Maasch, K.A., David Meeker, L., Meyerson, E.A., Gasse, F., Drinia, H., Anastasakis, G., Agiadi, K., Kafousia, N., De van Kreveld, S., Holmgren, K., Lee-Thorp, J., Rosqvist, G., Rafelis, M., 2016a. New insights into the early Pliocene hydro- Rack, F., Staubwasser, M., Schneider, R.R., Steig, E.J., 2004. graphic dynamics and their relationship to the climatic evolution Holocene climate variability. Quaternary Research, 62: of the Mediterranean Sea. Palaeogeography, Palaeoclimato- 243–255. logy, Palaeoecology, 459: 348–364. Meckler, A.N., Schubert, C.J., Hochuli, P.A., Plessen, B., Birgel, Kontakiotis, G., Mortyn, P.G., Antonarakou, A., Drinia, H., 2016b. D., Flower, B.P., Hinrichs, K.U., Haug, G.H., 2008. Glacial to Assessing the reliability of foraminiferal Mg/Ca thermometry by Holocene terrigenous organic matter input to sediments from comparing field-samples and culture experiments: a review. Orca Basin, Gulf of Mexico – a combined optical and biomarker Geological Quarterly, 60 (3): 547–560. approach. Earth and Planetary Science Letters, 272: 251–263. 190 Assimina Antonarakou et al. Metcalfe, S.E., O’Hara, S.L., Caballero, M., Davies, S.J., 2000. Putrasahan, D.A., Kamenkovich, I., Le Hénaff, M., Kirtman, B.P., Records of Late Pleistocene–Holocene climatic change in Mex- 2017. Importance of ocean mesoscale variability for air-sea in- ico — a review. Quaternary Science Reviews, 19: 699–721. teractions in the Gulf of Mexico. Geophysical Research Letters, Minisini, D., Trincardi, F., Asioli, A., Canu, M., Foglini, F., 2007. 44: 6352–6362. Morphologic variability of exposed mass-transport deposits on Rasmussen, T.L., Thomsen, E., 2012. Changes in planktic the eastern slope of Gela Basin (Sicily channel). Basin Re- foraminiferal faunas, temperature and salinity in the Gulf Stream search, 19: 217–240. during the last 30,000 years: influence of meltwater via the Mis- Montero-Serrano, J.C., Bout-Roumazeilles, V., Tribovillard, N., sissippi River. Quaternary Science Reviews, 33: 42–54. Sionneau, T., Riboulleau, A., Bory, A., Flower, B., 2009. Sedi- Renaud, S., Schmidt, D.N., 2003. Habitat tracking as a response of mentary evidence of deglacial megafloods in the northern Gulf the planktic foraminifer Globorotalia truncatulinoides to environ- of Mexico (Pigmy Basin). Quaternary Science Reviews, 28: mental fluctuations during the last 140 kyr. Marine Micropaleon- 3333–3347. tology, 49: 97–122. Montero-Serrano, J.C., Bout-Roumazeilles, V., Sionneau, T., Reynolds, C.E., Richey, J.N., Fehrenbacher, J.S., Rosenheim, Tribovillard, N., Bory, A., Flower, B.P., Riboulleau, A., Marti- B.E., Spero, H.J., 2018. Environmental controls on the geo- nez, P., Billy, I., 2010. Changes in precipitation regimes over chemistry of Globorotalia truncatulinoides in the Gulf of Mexico: North America during the Holocene as recorded by mineralogy implications for paleoceanographic reconstructions. Marine and geochemistry of Gulf of Mexico sediments. Global and Micropaleontology, 142: 92–104. Planetary Change, 74: 132–143. Richey, J.N., Poore, R.Z., Flower, B.P., Quinn, T.M., 2007. 1400 yr Montero-Serrano, J.C., Bout-Roumazeilles, V., Carlson Anders, multiproxy record of climate variability from the northern Gulf of E., Tribovillard, N., Bory, A., Meunier, G., Sionneau, T., Mexico. Geology, 35: 423–426. Flower Benjamin, P., Martinez, P., Billy, I., Riboulleau, A., Richey, J.N., Hollander, D.J., Flower, B.P., Eglinton, T.I., 2011. 2011. Contrasting rainfall patterns over North America during Merging late Holocene molecular organic and foramini- the Holocene and Last Interglacial as recorded by sediments of feral-based geochemical records of sea surface temperature in the northern Gulf of Mexico. Geophysical Research Letters, 38, the Gulf of Mexico. Paleoceanography, 26, PA1209, doi: L14709, doi: 10.1029/2011GL048194 10.1029/2010PA002000 Morard, R., Quillévéré, F., Escarguel, G., Ujiie, Y., de Garidel- Richey, J.N., Poore, R.Z., Flower, B.P., Hollander, D.J., 2012. Thoron, T., Norris, R.D., de Vargas, C., 2009. Morphological Ecological controls on the shell geochemistry of pink and white recognition of cryptic species in the planktonic foraminifer Globigerinoides ruber in the northern Gulf of Mexico: implica- Orbulina universa. Marine Micropaleontology, 71: 148–165. tions for paleoceanographic reconstruction. Marine Micropale- Morey, S.L., Martin, P.J., O’Brien, J.J., Wallcraft, A.A., Zavala-Hi- ontology, 82–83: 28–37. dalgo, J., 2003a. Export pathways for river discharged fresh Rohling, E.J., Jorissen, F.J., Grazzini, C.V., Zachariasse, W.J., water in the northern Gulf of Mexico. Journal of Geophysical Re- 1993. Northern Levantine and Adriatic Quaternary planktic search: Oceans, 108 (C10), 3303, doi: 10.1029/2002JC001674 foraminifera; Reconstruction of paleoenvironmental gradients. Morey S.L., Schroeder William, W., O’Brien James, J., Marine Micropaleontology, 21: 191–218. Zavala-Hidalgo, J., 2003b. The annual cycle of riverine influ- Rouis-Zargouni, I., Turon, J.-L., Londeix, L., Essallami, L., ence in the eastern Gulf of Mexico basin. Geophysical Research Kallel, N., Sicre, M.-A., 2010. Environmental and climatic Letters, 30 (16), 1867, doi: 10.1029/2003GL017348 changes in the central Mediterranean Sea (Siculo–Tunisian Müller-Karger, F.E., Walsh, J.J., Evans, R.H., Meyers, M.B., Strait) during the last 30ka based on dinoflagellate cyst and 1991. On the seasonal phytoplankton concentration and sea planktonic foraminifera assemblages. Palaeogeography, surface temperature cycles of the Gulf of Mexico as determined Palaeoclimatology, Palaeoecology, 285: 17–29. by satellites. Journal of Geophysical Research: Oceans, 96: Ruddiman, W.F., 1971. Pleistocene Sedimentation in the Equatorial 12645–12665. Atlantic: Stratigraphy and Faunal Paleoclimatology. GSA Bulle- Nürnberg, D., Ziegler, M., Karas, C., Tiedemann, R., Schmidt, tin, 82: 283–302. M.W., 2008. Interacting Loop Current variability and Mississippi Saha, K., 2010. Large-Scale Tropical Circulations. Springer, Berlin, River discharge over the past 400 kyr. Earth and Planetary Sci- Heidelberg. ence Letters, 272: 278–289. Sbaffi, L., Wezel, F.C., Curzi, G., Zoppi, U., 2004. Millennial- to Oey, L., Ezer, T., Lee, H., 2013. Loop Current, rings and related cir- centennial-scale palaeoclimatic variations during Termination I culation in the Gulf of Mexico: a review of numerical models and and the Holocene in the central Mediterranean Sea. Global and future challenges, circulation in the Gulf of Mexico: observations Planetary Change, 40: 201–217. and models. Geophysical Monograph Series, 161: 31–56. Schmidt, D.N., Renaud, S., Bollmann, J., Schiebel, R., Thier- Ohlmann, J.C., Niiler, P.P., Fox, C.A., Leben, R.R., 2001. Eddy en- stein, H.R., 2004a. Size distribution of Holocene planktic ergy and shelf interactions in the Gulf of Mexico. Journal of Geo- foraminifer assemblages: biogeography, ecology and adapta- physical Research: Oceans, 106: 2605–2620. tion. Marine Micropaleontology 50: 319–338. Patterson, R.T., Fishbein, E., 1989. Re-examination of the statisti- Schmidt, D.N., Thierstein, H.R., Bollmann, J., Schiebel, R., cal methods used to determine the number of point counts 2004b. Abiotic forcing of plankton evolution in the Cenozoic. needed for micropaleontological quantitative research. Journal Science 303: 207–210. of Paleontology, 63: 245–248. Schmidt, M.W., Spero, H.J., Lea, D.W., 2004. Links between salin- Poore, R.Z., Dowsett, H.J., Verardo, S., Quinn, T.M., 2003. Millen- ity variation in the Caribbean and North Atlantic thermohaline nial- to century-scale variability in Gulf of Mexico Holocene cli- circulation. Nature, 428: 160–163. mate records. Paleoceanography, 18, 1048, doi: Schmidt, M.W., Lynch-Stieglitz, J., 2011. Florida Straits deglacial 10.1029/2002PA000868 temperature and salinity change: Implications for tropical Poore, R.Z., Quinn, T.M., Verardo, S., 2004. Century-scale move- hydrologic cycle variability during the Younger Dryas. ment of the Atlantic Intertropical Convergence Zone linked to Paleoceanography, 26, PA4205, doi: 10.1029/21011PA002157 solar variability. Geophysical Research Letters, 31, L12214, doi: Schmidt, M.W., Weinlein, W.A., Marcantonio, F., Lynch-Stieglitz, 10.1029/2004GL019940 J., 2012. Solar forcing of Florida Straits surface salinity during Poore, R.Z., Pavich, M.J., Grissino-Mayer, H.D., 2005. Record of the early Holocene. Paleoceanography, 27. the North American southwest monsoon from Gulf of Mexico Schmitz, J.W.J., Biggs, D.C., Lugo-Fernandez, A., Oey, L.Y., sediment cores. Geology, 33: 209–212. Sturges, W., 2013. A Synopsis of the Circulation in the Gulf of Poore, R.Z., Tedesco, K.A., Spear, J.W., 2013. Seasonal flux and Mexico and on its Continental Margins. In: Circulation in the Gulf Assemblage composition of planktic foraminifers from a sedi- of Mexico: Observations and Models (eds. W. Sturges and ment-trap study in the Northern Gulf of Mexico. Journal of A. Lugo-Fernandez): 11–29. American Geophysical Union, Coastal Research: 6–19. Washington, D.C. Eco-biostratigraphic advances in late Quaternary geochronology and palaeoclimate: the marginal Gulf of Mexico analogue 191 Schmuker, B., Schiebel, R., 2002. Planktic foraminifers and cial–Holocene ecostratigraphy of the south-eastern Aegean hydrography of the eastern and northern Caribbean Sea. Marine Sea, based on plankton and pollen assemblages. Geo-Marine Micropaleontology, 46: 387–403. Letters, 29: 249–267. Shakun, J.D., Raymo, M.E., Lea, D.W., 2016. An early Pleistocene Tripsanas, E.K., Bryant, W.R., Slowey, N.C., Bouma, A.H., Mg/Ca-d18O record from the Gulf of Mexico: evaluating ice sheet Karageorgis, A.P., Berti, D., 2007. Sedimentological history of size and pacing in the 41-kyr world. Paleoceanography, 31, doi: Bryant Canyon area, northwest Gulf of Mexico, during the last 10.1002/2016PA002956. 135 kyr (Marine Isotope Stages 1–6): a proxy record of Missis- Siani, G., Paterne, M., Colin, C., 2010. Late glacial to Holocene sippi River discharge. Palaeogeography, Palaeoclimatology, planktic foraminifera bioevents and climatic record in the South Palaeoecology, 246: 137–161. Adriatic Sea. Journal of Quaternary Science, 25: 808–821. Tripsanas, E.K., Karageorgis, A.P., Panagiotopoulos, I.P., Sionneau, T., Bout-Roumazeilles, V., Biscaye, P.E., Van Koutsopoulou, E., Kanellopoulos, T.D., Bryant, W.R., Vliet-Lanoe, B., Bory, A., 2008. Clay mineral distributions in Slowey, N.C., 2013. Paleoenvironmental and paleoclimatic im- and around the Mississippi River watershed and Northern Gulf plications of enhanced Holocene discharge from the Mississippi of Mexico: sources and transport patterns. Quaternary Science river based on the sedimentology and geochemistry of a deep Reviews, 27: 1740–1751. core (JPC-26) from the Gulf of Mexico. PALAIOS, 28: 623–636. Sionneau, T., Bout-Roumazeilles, V., Flower, B.P., Bory, A., Vetter, L., Spero, H.J., Eggins, S.M., Williams, C., Flower, B.P., Tribovillard, N., Kissel, C., Van Vliet-Lanoë, B., Montero 2017. Oxygen isotope geochemistry of Laurentide ice-sheet Serrano, J.C., 2010. Provenance of freshwater pulses in the meltwater across Termination I. Quaternary Science Reviews, Gulf of Mexico during the last deglaciation. Quaternary Re- 178: 102–117. search, 74: 235–245. Wang, C., Enfield, D., B., 2001. The tropical western hemisphere Spear, J.W., Poore, R.Z., Quinn, T.M., 2011a. Globorotalia trunca- warm pool. Geophysical Research Letters, 28: 1635–1638. tulinoides (dextral) Mg/Ca as a proxy for Gulf of Mexico winter Wawrik, B., Paul, J.H., Campbell, L., Griffin, D., Houchin, L., mixed-layer temperature: Evidence from a sediment trap in the Fuentes-Ortega, A., Muller-Karger, F., 2003. Vertical structure northern Gulf of Mexico. Marine Micropaleontology, 80: 53–61. of the phytoplankton community associated with a coastal Spear, J.W., Reynolds, C.E., Poore, R.Z., 2011b. Seasonal Flux plume in the Gulf of Mexico. Marine Ecology Progress Series, and Assemblage Composition of Planktic Foraminifera from the 251: 87–101. Northern Gulf of Mexico, 2008–2009. U.S. Geological Survey Weisberg, R.H., Liu, Y., 2017. On the Loop Current penetration into Open-File Report, 2011–1002. the Gulf of Mexico. Journal of Geophysical Research: Oceans, Sprovieri, R., Di Stefano, E., Incarbona, A., Gargano, M.E., 2003. 122: 9679–9694. A high-resolution record of the last deglaciation in the Sicily Wejnert, K.E., Pride, C.J., Thunell, R.C., 2010. The oxygen iso- Channel based on foraminifera and calcareous nannofossil tope composition of planktonic foraminifera from the Guaymas quantitative distribution. Palaeogeography, Palaeoclimatology, Basin, Gulf of California: Seasonal, annual, and interspecies Palaeoecology, 202: 119–142. variability. Marine Micropaleontology, 74: 29–37. Sprovieri, R., Di Stefano, E., Incarbona, A., Oppo, D.W., 2006a. Weldeab, S., Schneider, R.R., Kölling, M., 2006. Deglacial sea Suborbital climate variability during Marine Isotopic Stage 5 in surface temperature and salinity increase in the western tropical the central Mediterranean basin: evidence from calcareous Atlantic in synchrony with high latitude climate instabilities. plankton record. Quaternary Science Reviews, 25: 2332–2342. Earth and Planetary Science Letters, 241: 699–706. Sprovieri, R., Sprovieri, M., Caruso, A., Pelosi, N., Bonomo, S., Williams, C., Flower Benjamin, P., Hastings David, W., Ferraro, L., 2006b. Astronomic forcing on the planktonic Guilderson Thomas, P., Quinn Kelly, A., Goddard Ethan, A., foraminifera assemblage in the Piacenzian Punta Piccola sec- 2010. Deglacial abrupt climate change in the Atlantic Warm tion (southern Italy). Paleoceanography, 21, PA4204, Pool: a Gulf of Mexico perspective. Paleoceanography, 25, doi:10.1029/2006PA001268 PA4221, doi: 10.1029/2010PA001928 Sprovieri, M., Di Stefano, E., Incarbona, A., Salvagio Manta, D., Williams, D.F., Kohl, B., 1986. Isotope chronostratigraphy and car- Pelosi, N., Ribera d’Alcal´, M., Sprovieri, R., 2012. Centen- bonate record for quaternary site-619, Pygmy Basin, Louisiana nial- to millennial-scale climate oscillations in the Central-East- continental-slope. Initial Reports of the Deep Sea Drilling Pro- ern Mediterranean Sea between 20,000 and 70,000 years ago: ject: 671–676. evidence from a high-resolution geochemical and micropale- Wilson, B., 2012. Biogeography and ecostratigraphy of Late Qua- ontological record. Quaternary Science Reviews, 46: 126–135. ternary planktonic foraminiferal taphocoenoses in the Leeward Tedesco, K.A., Thunell, R.C., 2003. Seasonal and interannual vari- Islands, Lesser Antilles, NE Caribbean Sea. Marine Micro- ations in Planktonic Foraminiferal flux and assemblage compo- paleontology, 86–87: 1–10. sition in the Cariaco Basin, Venezuela. Journal of Foraminiferal Wilson, J.D., Monteiro, F.M., Schmidt, D.N., Ward, B.A., Research, 33: 192–210. Ridgwell, A., 2018. Linking marine plankton ecosystems and Tedesco, K., Thunell, R., Astor, Y., Muller-Karger, F., 2007. The climate: A new modeling approach to the warm early Eocene cli- oxygen isotope composition of planktonic foraminifera from the mate. Paleoceanography and Paleoclimatology, 33, Cariaco Basin, Venezuela: seasonal and interannual variations. doi.org/10.1029/2018PA003374 Marine Micropaleontology, 62: 180–193. Zarkogiannis, S.D., Kontakiotis, G., Antonarakou, A., Mortyn, Thirumalai, K., Richey, J.N., Quinn, T.M., Poore, R.Z., 2014. P.M., Drinia, H., 2019a. Latitudinal variation of planktonic Globigerinoides ruber morphotypes in the Gulf of Mexico: a test foraminifera shell masses during Termination I. IOP Conference of null hypothesis. Scientific Reports, 4, 6018: 1–7. Series: Earth and Environmental Sciences, 221: 012052 Thirumalai, K., Quinn, T.M., Okumura, Y., Richey, J.N., Partin, doi:10.1088/1755-1315/221/1/012052 J.W., Poore, R.Z., Moreno-Chamarro, E., 2018. Pronounced Zarkogiannis, S.D., Antonarakou, A., Tripati, A., Kontakiotis, G., centennial-scale Atlantic Ocean climate variability correlated Mortyn, P.G., Drinia, H., Greaves, M., 2019b. Influence of sur- with Western Hemisphere hydroclimate. Nature Communica- face ocean density on planktonic foraminifera calcification. Sci- tions, 9: 392. entific Reports, 9: 533, doi: 10.1038/s41598-018-36935-7 Toner, M., Kirwan, A.D., Poje, A.C., Kantha, L.H., Müller-Karger, Zavala-Hidalgo, J., Morey, S.L., O’brien, J.J., Zamudio, L., 2006. F.E., Jones, C.K.R.T., 2003. Chlorophyll dispersal by eddy-eddy On the Loop Current eddy shedding variability. Atmósfera, 19: interactions in the Gulf of Mexico. Journal of Geophysical Re- 41–48. search: Oceans, 108 (C4), 3105, Ziegler, M., Nürnberg, D., Karas, C., Tiedemann, R., Lourens, http://dx.doi.org/10.1029/2002JC001499 L.J., 2008. Persistent summer expansion of the Atlantic Warm Triantaphyllou, M.V., Antonarakou, A., Kouli, K., Dimiza, M., Pool during glacial abrupt cold events. Nature Geoscience, 1: Kontakiotis, G., Papanikolaou, M.D., Ziveri, P., Mortyn, P.G., 601–605. Lianou, V., Lykousis, V., Dermitzakis, M.D., 2009. Late Gla-