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Brazilian Journal of Oceanography

versão On-line ISSN 1982-436X

Braz. j. oceanogr. vol.59 no.4 São Paulo out./dez. 2011

http://dx.doi.org/10.1590/S1679-87592011000400003 

Relationship between isotopic composition (Δ18O and Δ13C) and plaktonic foraminifera test size in core tops from the Brazilian Continental Margin

 

 

Paula Franco-Fraguas*; Karen Badaraco Costa; Felipe Antonio de Lima Toledo

Instituto Oceanográfico da Universidade de São Paulo (Praça do Oceanográfico, 191, 05508-120 São Paulo, SP, Brasil)

 

 


ABSTRACT

Stable oxygen (δ18O) and carbon (δ13C) isotopic signature registered in fossil planktonic foraminifera tests are widely used to reconstruct ancient oceanographic conditions. Test size is a major source of stable isotope variability in planktonic foraminifera found in sediment samples and thus can compromise paleoceanographic interpretations. Test size/stable isotope (δ18O and δ13C) relationships were evaluated in two planktonic foraminifer species (Globigerinoides ruber (white) and Globorotalia truncatulinoides (right)) in two core tops from the Brazilian Continental Margin. δ18 Omeasurements were used to predict the depth of calcification of each test size fraction. δ13C offsets for each test size fraction were then estimated. No systematic δ18O changes with size were observed in G. ruber (white) suggesting a similar calcification depth range (c.a. 100 m) during ontogeny. For G. truncatulinoides (right) δ18O values increased with size indicating ontogenetic migration along thermocline waters (250-400 m). δ13C measurements and δ13C offsets increased with size for both species reflecting well known physiological induced ontogenetic-related variability. In G. ruber (white) the largest test size fractions (300µm and >355µm) more closely reflect δ13CDIC indicating they are best suited for paleoceanographic studies.

Descriptors: Planktonic foraminifera, Stable isotopes, Test size.


RESUMO

O tamanho de testa dos foraminíferos é uma importante fonte de variabilidade isotópica (δ18O e δ13C) em amostras de sedimento marinho comprometendo as interpretações paloeceanograficas. No presente estudo, avaliou-se a relação entre o sinal isotópico medido em diferentes frações de tamanho de testa das espécies planctônicas, Globigerinoides ruber (branca) e Globorotalia truncatulinoides (dextral) em amostras de topo de dois testemunhos localizados na Margem Continental Brasileira. Os valores de δ18O foram utilizados para estimar a profundidade de calcificação de cada fração de tamanho. Os desequilíbrios nos valores de δ13C para cada fração de tamanho foram estimados. Os valores de δ18O em G. ruber (branca) não apresentaram tendência com o tamanho sugerindo que calcifica dentro de um mesmo intervalo de profundidade (c.a. 100 m) durante a ontogenia. Os valores de δ18O em G. truncatulinoides (dextral) apresentaram aumento com o tamanho refletindo a migração ontogênica em águas da termoclina (250-400 m). Os valores e desequilíbrios de δ13C aumentaram com o tamanho nas duas espécies indicando o efeito da variação nas taxas fisiológicas durante a ontogenia. Em G. ruber (white) os valores de δ13C dos maiores tamanhos (300µm e >355µm) refletem melhor os valores de δ13CDIC indicando que são mais apropriados para utilizar nas reconstruções paleoceanograficas.

Descritores: Foraminíferos planctônicos, Isótopos estáveis, Tamanho testas.


 

 

INTRODUCTION

During the calcification process, planktonic foraminifera record the stable isotope signature and environmental conditions of seawater of their calcification depth in a predictable way (ROHLING; COOKE, 1999). As a consequence, stable oxygen (δ18O) and carbon (δ13C) isotopes measured in tests of fossil planktonic foraminifera are widely used in paleoceanography as proxies for paleotemperature, ice volume, water masses movements and paleoproductivity (WEFER et al., 1999; ROHLING; COOKE, 1999). However, in some planktonic species measured stable isotope composition often shows offsets from predicted values (RAVELO; FAIRBANKS, 1995).

These offsets are associated with foraminiferal physiological processes such as respiration, calcification and photosynthesis (in symbiont bearing species) (SPERO; LEA, 1993; ZEEBE et al., 1999). The carbonate ion effect, associated with calcification processes, also induces offsets during calcification of δ13C and δ18O (SPERO et al., 1997). Both laboratory and field based (with living and fossil foraminifera) studies have demonstrated that these offsets are higher regarding δ13C than δ18O values. δ18O measurements in tests of recent planktonic foraminifera can thus be used to evaluate δ13C offsets (ELDERFIELD et al., 2002; RAVELO; FAIRBANKS, 1995).

Test size is a major source of stable isotope intra-specific variability found in sediment samples. Some of the stable isotopic offsets observed in planktonic foraminifera species are related to test size, having important implications when choosing foraminifera test size fractions for paleoceanographic interpretations (OPPO; FAIRBANKS, 1989). The size-related stable isotope variability can be caused by 1) variation in physiological rates during ontogeny (RAVELO; FAIRBANKS, 1995) and 2) variability in calcification depth during the life cycle (e.g., depth migrations along the water column; LOHMANN, 1995), and during different environmental conditions (e.g., different seasons; DEUSER et al., 1981).

The complexity of isotopic fractionation in foraminifera and its relationship with local environmental condition suggests the importance of evaluating size-related stable isotope variability in areas of paleoceanographic interest. Several authors have used stable isotopes measurements in planktonic foraminifera from the Brazilian Continental Margin as proxies for ancient hydrographic conditions (ARZ, 1998, 1999; TOLEDO et al., 2007). However, there are no local calibration studies concerning both sizerelated stable oxygen and carbon isotopes in planktonic foraminifera.

The most straightforward approach for the evaluation of paleoceanographic proxies is the analysis of core top samples and its relationship with modern hydrographic conditions. The present work explores sieve size-related stable isotope oxygen and carbon variability in two species of planktonic foraminifera, Globigerinoides ruber (white) and Globorotalia truncatulinoides (right), in two core tops from the Brazilian Continental Margin. Additionally, we estimated the depth of calcification reflected by measured δ18 values retained in each sieve size fraction and analyzed which test size fraction best reflects seawater carbon stable isotope signature in the previously estimated calcification depth.

 

MATERIALS AND METHODS

Cores and Oceanographic Context

We measured the oxygen and carbon isotopes of planktonic foraminifera from two piston core tops, KF-F and KF-G (Table 1) recovered from the Brazilian Continental Margin in the southwestern South Atlantic (Fig. 1).

 

 

 

 

The Brazilian southeastern margin is characterized by the stacking of several water masses, including Tropical Water (TW), South Atlantic Central Water (SACW), Antarctic Intermediate Water (AAIW), North Atlantic Deep Water (NADW) and the Antarctic Bottom Water (AABW). The surface waters result from the mixing of three water masses: the TW, a hot (T>18.8ºC) and high-salinity water (S> 36%), the coastal waters and the waters resulting from vertical excursions (upwelling) of the SACW (GARFIELD, 1990). The SACW is cooler (T<18.8ºC) and less saline (S<36%) (DUARTE; VIANA, 2007).

Chronology and Isotopic Measurements

Chronology was based on the correlation of the isotopic record of benthic foraminifera with SPECMAP chronology of Martinson et al. (1987) and on radiocarbon data using Accelerator Mass Spectrometer (AMS) radiocarbon dating performed on two samples of monospecific planktonic foraminifera (G. ruber) from the core top sample of each core (1cm -KF-F and 1.5cm -KF-G). The 14C-AMS dating were performed at NOSAMS-WHOI laboratory facility, and all the 14C ages were corrected for a reservoir effect of 400 yrs and transformed into calendar yrs (BARD, 1993).

Stable isotopes analyses were carried out at Woods Hole Oceanographic Institution, MA, USA using a Finnigan MAT253 mass spectrometer with the automated Kiel device. Isotope values are represented in standard δ notation relative to the Vienna Pee Dee Belemnite (VPDB) for calcite and Vienna StandardMean-Water (VSMOW) for sea water. Calibration of the PDB was done via the NBS-19 with an accuracy of ±0.07 for δ18O and ±0.03 for δ13C.

Sampling Procedure

Cores were previously sub-sampled every 510cm and samples washed with distilled water over a 63µm mesh size and dried at 50ºC. In order to work with Holocene samples, the three core top samples of each core with lower δ18O values (based on available Globigerionides ruber stable oxygen isotopes) were selected: 1cm, 6cm and 11cm from KF-F and 1.5cm, 9cm and 16cm from KF-G.

The samples were separated in the following sieve size fractions: 150-250µm, 250-300µm, 300355µm and >355µm according to availability of some of the more frequent sieve size fractions used in calibration (ELDERFIED et al., 2002; RAVELO; FAIRBANKS, 1992, 1995) and reconstruction (ARZ et al., 1998, 1999; TOLEDO et al., 2007) studies. The surface dwelling G. ruber (white) and the deep dwelling Globorotalia truncatulinoides (right) species were identified based on Van Morkoven et al. (1986) and Hemleben et al. (1989). Stable isotope measurements were conducted on between three and six G. ruber (white) tests and on between three and four G. truncatulinoides (right) tests depending on the size fraction. In KF-F, 4 replicates samples of G. ruber (white) were analyzed in the 150-250µm and 250-300 µm size classes allowing evaluation of within size fraction variability. The largest individuals of each size fraction were picked to improve sample comparison. Tests with apparent good preservation (e.g., without fragmentation and color or texture modification) were picked and samples with apparent attached sediments were washed by ultrasonification.

Stable Isotope / Test Size Relationship

The effect of size fraction on each species for both corers was evaluated by a one-way analysis of variance (ANOVA). The Kolmogorov-Smirnov D statistic was used to check for normality, while Cochran's C-test was used to check the assumption of homogeneity of variances. In cases where homogeneity was not achieved, we set the critical level to a value equal to the p-value for variance homogeneity (UNDERWOOD, 1997). All analyses were performed separately for both isotopic values of each species.

Hydrographic Data and Isotopic Composition in the Water Column

Hydrographic data (annual temperature and salinity) along the surface water masses from two stations next to each core top location were extracted from the World Ocean Atlas, 2005 (WOA05) (LOCARNINI et al., 2006; ANTONOV et al., 2006) and are henceforth called WOAKF-F and WOAKF-G for proximity to cores KF-F and KF-G, respectively (Fig. 1). These data was used to identify surface water masses and for estimating oxygen stable isotope values in seawater (δ18OW) and in equilibrium with seawater (δ18OEQ). Water masses and mixed layer limits were based on Silveira et al. (2000) and Tomczak and Godfrey (1994), respectively.

δ18OW values were estimated based on annual salinity WOA05 data and δ18O/salinity equations from Legrand and Schmidt (2006). Tropical Atlantic (eq. 1) and South Atlantic (eq. 2) equations (LEGRAND; SCHMIDT, 2006) were used to estimate δ18OW for TW and SACW water masses, respectively.

where δ18OW= δ18O of seawater (VSMOW, %) and S = salinity (%)

Predicted Stable Isotope Values and relationship with the Isotopic Measurements in Foraminifera

Planktonic foraminifera dwell and calcify their carbonate tests at the surface of the water column. Foraminiferal δ18O measurements are assumed to be principally a function of stable isotope signature in seawater (δ18OW) and temperature. Thus, comparison of δ18 O measurements in core top planktonic tests with predicted values of calcite in equilibrium with modern seawater (δ18OEQ) (obtained from paleotemperature equations) will provide information about the calcification depth of each species (RAVELO; FAIRBANKS, 1992; NIEBLER et al., 1999).

We estimated calcite precipitated in isotopic equilibrium with seawater (δ18OEQ) based on δ18OW values, annual temperature (WOA05) and using well known paleotemperature equations (see below). δ18OEQ (VSMOW) were converted to δ18OEQ (VPDB) values after HUT (1987) equation.

Different inorganic paleotemperature equations have been proposed for calibration and paleoceanographic purposes (SHACKLETON, 1974; KIM; O'NEIL, 1997). Spero et al. (1997) demonstrated that besides temperature, ambient carbonate ion concentration also influence δ18Ocalcification in foraminifera. Mulitza et al. (2003) calibrated a new paleotemperature equation using living surface dwelling foraminifera (including G. ruber). This paleotemperature equation takes into consideration surface seawater carbonate ion concentration influence on δ18O measurements. Hence, comparison of δ18O measurements in surface dwelling foraminifera (e.g., G. ruber) with predicted δ18O of calcite in equilibrium with seawater (δ18OEQ) based on Mulitza et al. (2003) in a more appropriate estimation of the calcification depth for this species. Thereafter, Mulitza et al. (2003) paleotemperature equation (eq. 3) was used to estimate depth of calcification of G. ruber (white). Kim and O'Neil (1997) and Mulitza et al. (2003) paleotemperature equations do not differ significantly at thermocline depth (MULITZA et al., 2003). Thus, in order to allow comparisons with other studies based on paleotemperature inorganic equations, Kim and O'Neil (1997) paleotemperature equation (eq. 4) was used to estimate G. truncatulinoides (right) depth of calcification.

where T = temperature (ºC), δ18O = predicted δ18O of calcite in equilibrium with seawater (VSMOW,%) and δ18Ow= δ18O of seawater (VSMOW, %).

δ13C equilibrium fractionation and its temperature dependence are still in debate. While Emrich et al. (1970) and Romanek et al. (1992) proposed temperature-dependent and temperatureindependent equilibrium equations, respectively, different calibrating studies use δ13CDIC to predict seawater values (ELDERFIELD et al., 2002). For evaluation of δ13C offsets in planktonic foraminifera we choose the third approach. δ13CDIC values were obtained from GEOSECS (station 55; 18ºS, 31ºW) (BAINDBRIDGE, 1981) close to core locations (Fig. 1).

For both species, δ18O measurements in foraminiferal tests were used to predict the calcification depth for each test-size fraction, and therefore the δ13C of dissolved inorganic carbon of seawater (δ13CDIC). The δ13C values in foraminifera are assumed to reflect the δ13C values of the seawater of calcification and probably physiological effects. Thus, offsets from predicted values of each test size fraction were calculated subtracting δ13C measured values from the predicted values at the depth of calcification. Only AMS radiocarbon Holocene-dated foraminifera samples (Table 2) were used to compare to surface water δ18OEQ and δ13CDIC values.

 

 

RESULTS

Isotopic Composition of Water Column

Hydrographic data and stable isotopic values in seawater are presented in Table 3. TW and SACW limit was established at 150 m. On an annual basis, temperature mixed layer limit was ca. 50 m. Thermocline waters ranged from the mixed layer limit down to ca. 1000 m. δ18OW decreased along the water column reflecting the relatively high evaporation in surface waters. δ18OEQ increased with depth according to the decrease in temperature. Higher δ18OEQ values at WOAKF-G with respect to WOAKF-F reflects its southernmost location along the Brazilian Continental Margin. Mixed layer δ18OEQ values estimated using Mulitza et al. (2003) paleotemperature equation ranged between -2.12% and -1.98% in WOAKF-F and between -1.88% and -1.67% in WOAKF-G (Table 3). Thermocline (depth>50 m) δ18OEQ values estimated using Kim and O'Neil (1997) equation showed minima of -1.39% and -1.12% values in WOAKF-F and WOAKF-G, respectively. Mixed layer δ13CDIC value was 1.9% and decreased with depth (Table 3), mirroring nutrient water profile.

Foraminifera oxygen stable isotopes

All stable isotope results are presented in Table 4. Maximum δ18O variability within a same G. ruber (white) size fraction (250-300µm) was 0.72%. There were no systematic changes in δ18O with size for G. ruber (white) (Figure 2a, ANOVA; F (3, 38) = 0.895, p >0.05). Systematic increment in δ18O with size for G. ruber (white) (Fig. 2a, ANOVA; F (3, 38) = 0.895, p >0.05). Systematic increment in δ18O with size was evident for G. truncatulinoides (Fig. 2a, ANOVA; F (3, 20) = 3.686, p < 0.05).

Comparison of G. ruber (white) δ18O measurements in 1cm (KF-F) and 1.5cm (KF-G) with predicted δ18OEQ values for surface water above each core top location using Mulitza et al. (2003) (M) equation indicates a depth of calcification of ca. 100 m (Fig. 3a, b). Depth of calcification for G. truncatulinoides (right) using Kim and O'Neil (1997) paleotemperature equation (KO) was ca. 250 m for the smallest size fraction (150-250µm) and between 250 m (KF-G) and 400 m (KF-F) for the largest size fraction (>355µm) (Fig. 3a, b).

Foraminifera Carbon Stable Isotopes

Maximum G. ruber (white) δ13C variability within a size fraction (KF-F; 150-250µm) was 0.62%. G. ruber (white) δ13C measurements increased with size (Fig. 2b, ANOVA; F (3, 38) = 36.36, p < 0.01) with a maximum δ13C difference of 1.85% between extreme size fractions (KF-F; 1cm). G. truncatulinoides (right) δ13C also increased with size (Fig. 2b, ANOVA; F (3, 20) = 15.73, p <0.01) with maximum variation of 1.26% between extreme size fractions (KF-F; 6cm). G. truncatulinoides (right) show lighter δ13C values than G. ruber (white) (Fig. 2b).

Offsets from predicted values increased with size fractions for both species (Fig. 4a, b). For G. ruber (white) δ13C measurements in the largest size fractions (300-355μm and >355μm) are closer to δ13CDIC values in the corresponding depth of calcification (offset ≈ 0) (Fig. 4a). Concerning G. truncatulinoides (right), the largest size fractions seem to present lower offsets, although this was not so clear (Fig. 4b).

 

DISCUSSION

Comparison of Core top Samples with Modern Hydrographic Conditions

Even though all samples reflect Holocene surface water conditions, only dated samples were used for comparison with modern hydrological conditions. Comparison of modern hydrographic data and core-top samples may have some methodological limitations concerning time scales. While modern WOA05 data represent mean hydrological conditions from the last decades, core tops used in this study reflect late Holocene conditions, i.e. 1357kyr (KF-F) and 3482kyr (KF-G). However, several authors suggested relatively weak upper water column hydrographic changes during the Holocene from the Brazilian Continental Margin (ARZ, 1998; TOLEDO et al., 2007). Moreover, this approach is commonly used for core top isotopic calibration studies worldwide (RAVELO; FAIRBANKS, 1992, 1995; ELDERFIELD et al., 2002; MULITZA et al., 2003; WAELBROECK et al., 2005).

Stable Isotope (δ18O and δ13C) Variability Within a Single Size Fraction

Several factors can influence δ18O planktonic foraminifera intra-specific variability; variable depth and season of calcification (MULITZA et al., 2003); variable calcification, respiration and photosynthesis rates (WOLF-GLADROW et al., 1999); amount of secondary calcification (HEMLEBEN et al., 1989); different morphotypes (LOWEMARK et al., 2005); dissolution (LOHMANN, 1995) and bioturbation (MULITZA et al., 2003). Regarding δ13C values, the variability in depth and season of calcification as well as variable calcification, respiration and photosynthesis rates (WOLF-GLADROW et al., 1999) can result in important intra-specific variability.

Paleoceanographic interpretations are usually based on a single test size fraction. However, since intra-specific variability is inversely related to the amount of foraminifera tests used per stable isotopic analysis (WAELBROECK et al., 2005), the use of as many tests as possible per isotope analysis (e.g., ca. 20 tests per analysis) (WAELBROECK et al., 2005) has been suggested. This should decrease the stable isotope variability within a single size fraction and identify the average stable isotope signature of a fossil population.

In this study, the maximum intra-specific variability found within replicates of a single size fraction for G. ruber (white) using 4-6 tests per analysis was 0.72% for δ18O (KF-F; 250-300μm) and 0.62% for δ13C (KF-F; 150-250μm). These results are in agreement with equatorial Pacific G. ruber studies using single test analysis (e.g., 2%, 250-350μm for δ18O and δ13C) (WAELBROECK et al., 2005). During calcification a δ18O increment of 0.25% accounts for a diminution of 1ºC for ambient seawater temperature (ROHLING; COOKE, 1999), whereas during δ13C calcification an increment of 1% accounts for a decrease of 1μmol/kg for ambient phosphate (BROECKER; MAIER-REIMER, 1992). This reflects the importance of increasing the amount of tests used in isotopic analyses when searching for the true average value of each size fraction and/or single sample in the region. The use of a relatively small amount of tests per stable isotope analysis in this study may preclude conclusive stable isotope/test size relationship. However, this was partially solved

δ18O/test Size Relationship

Studies concerning δ18O/test size relationship in the shallow dwelling G. ruber in recent sediment samples along a complete range of test sizes show either a decrease with size (KROON; DARLING, 1995), a slight increase with size (BERGER et al., 1978) or no systematic changes with size (ELDERFIELD et al., 2002; WAELBROECK et al., 2005). The decrease with size was explained as local seasonal environmental factors (irradiance, salinity and/or temperature) affecting both size and stable isotope signature of G. ruber (KROON; DARLING, 1995). The increase with size was suggested to reflect the development of adult secondary calcification in cold deeper waters (DUPLESSY et al., 1981). The lack of systematic δ18O/test size variation observed for G. ruber (white) suggests that in the study area this species calcify without environmentally-induced test size and stable isotope variations and/or along a similar range of depths during ontogeny.

G. trunatulinoides is a deep dwelling species which undergoes vertical migration during its ontogeny (HEMLEBEN et al., 1989; LOHMANN, 1995). This implies the calcification of an ontogenetic calcite test in shallow, warmer waters during juvenile stages and a secondary calcification crust in deeper, cooler waters during adult stages (HEMLEBEN et al., 1989). Thereafter, G. truncatulinoides incorporates a lighter and heavier δ18O signature during primary and secondary calcification, respectively (LOHMANN, 1995; MULITZA et al., 1997). However, its bulk test chemistry is a mixture of two end-member calcite and depends on the relative proportion of each calcite (LOHMANN, 1995). In this work it was not intended to identify calcification crust. Hence, the systematic δ18O increase with size fraction reflect migratory behavior.

Apparent depth of calcification

Several studies have demonstrated the potential of δ18O measurements in core top planktonic foraminifera to reflect species' calcification depth (NIEBLER et al., 1999; RAVELO; FAIRBANKS, 1992). Plankton studies demonstrated that the symbiont-bearing G. ruber (white) is a surface dwelling species associated with the mixed surface layer (KEMLE-VON MUCKE; OBERHANSLI, 1999). In the region, the depth of maximum G. ruber density (0-40 m; Sorano, pers. com.) is coincident with the estimated annual mixed layer depth (ca. 50 m). The reflected depth of calcification here estimated (ca. 100 m) agreed with previous reported data from the region (CHIESSI et al., 2007) based on annual temperature and the same paleotemperature equation. The difference between this estimated depth of calcification and the plankton habitat depth may be due to seasonal flux, vertical migration and/or postdepositional effects (MULITZA et al., 2003). However, since seasonal flux in this species seems to occur mainly during summer this should be reflected in a sediment mean flux-weighed shift towards lighter than annual mean δ18O values (MULITZA et al., 2003), thus making this explanation improbable. Although dissolution effects are unlikely because of the relatively shallow sampling water depth (ca. 2000 m) with respect to lysocline depth in the modern South Atlantic ocean (ca. 4100 m; FRENZ; HENRICH, 2007), bioturbation may occur in areas of low sedimentation rates such as the study region (3cm/1000kyr, TOLEDO et al., 2005). Nonetheless, differences between living and sediment G. ruber (white) δ18O measurements (0.5-1.0%) were also observed in global studies (MULITZA et al., 2003; WAELBROECK et al., 2005) discarding late Holocene samples with possible bioturbation. In this paper, δ18O / sieve size relationship suggests G. ruber (white) calcification along a similar depth range during ontogeny, while Mulitza et al. (2003) and Waelbroeck et al. (2005) suggest calcification in deeper waters during ontogenesis or gametogenesis as a probable explanation of this observed isotopic difference. This difference seems to be higher in low latitudes where stratification of the water column is more pronounced and in areas of low surface salinity (WAELBROECK et al., 2005). These authors stated that the relationship between δ18O equilibrium calcite and δ18O from sediment planktonic foraminifera is complex and depends on local hydrography. Therefore, differences between plankton and sediment G. ruber δ18O values must be taken into account during paleoceanographic interpretations based on sediment samples (WAELBROECK et al., 2005).

For the deep dwelling G. truncatulinoides (right) the depth of calcification estimated agree with Mulitza et al. (1997) for tropical waters and suggests primary calcification below the highly stratified mixed layer waters (ca. 250 m) and adult calcification of a secondary crust in deeper cold waters (ca. 400 m). Moreover, this adult calcification depth coincides with the temperature known to trigger the calcification of the secondary crust (8-10ºC, HEMLEBEN et al., 1989).

δ13C/test Size Relationship and δ13C offsets

The increase δ13C with size observed in G. ruber (white) and G. truncatulinoides (right) is well known in other regions in both plankton (WILLIAMS et al., 1981; DUPLESSY et al., 1981) and sediment samples (HEMLEBEN et al., 1989; RAVELO; FAIRBANKS, 1995; ELDERFIELD et al., 2002). This increase is commonly explained invoking different rates of calcification, respiration and photosynthesis (in symbiotic species) along foraminiferal ontogeny. These factors influence the chemistry of the microenvironment of foraminifera and hence the δ13C registered in the tests (ZEEBE et al., 1999; WOLF-GLADROW et al., 1999). For G. truncatulinoides (right) this increase opposed the seawater δ13CDIC gradient (decrease with depth) contradicting the depth of calcification reflected by δ18O values. The highest δ13C values observed in G. ruber (white) compared with G. truncatulinoides in size fractions agree with other studies (WILLIAMS et al. 1981; RAVELO; FAIRBANKS, 1995) and likely reflects calcification of G. ruber in shallower waters.

Physiological effects result in size-dependent offsets from predicted δ13C values, suggesting the need to limit test size fractions used in paleoceanographic studies. Ravelo and Fairbanks (1995) observed G. ruber (white) δ13C offsets varied with regional hydrography although they attributed it to uncertainties in seawater δ13CDIC values. The use of small amount of tests per analysis in the largest size fractions together with scarce δ13CDIC values available in the region precludes evaluating differences in δ13C offsets between core tops. However, it is clear that δ13C measurements of the largest size fractions (300355µm and >355µm) of G. ruber (white) are closer to predicted δ13CDIC values from the estimated depths of calcification. This agree with Elderfield et al. (2002) and Ravelo and Fairbanks (1995) and indicates that physiological size-related effects decrease with size and/or that opposed physiological effects cancel each other in the largest test size fractions. Thus, the largest test size fractions of G. ruber (white) are more adequate for paleoceanographic interpretations based on δ13C measurements. For G. truncatulinoides (right) δ13C offsets also vary with test size indicating physiological size-related influence on δ13C offsets. Elderfield et al. (2002) observed that the largest size fractions of G. truncatulinoides were closer to predicted δ13CDIC values in the depth of calcification. In this work this was not so clear. This suggests that other factors than size-related physiological effects are influencing δ13C offsets in G. truncatulinoides. This line up with Ravelo and Fairbanks (1995) who observed size-related offsets even using a larger amount of G. truncatulinoides tests per analysis. They demonstrated that temperature also affects δ13C offsets in G. truncatulinoides (right) showing the complexity in G. truncatulinoides δ13C fractionation.

 

CONCLUSIONS AND PALEOCEANOGRAPHIC IMPLICATIONS

Despite limitations due to the use of relatively small amount of tests per analysis and limited local δ13CDIC values, measurements of isotopic composition (δ18O and δ13C) of sieve test size fractions of two planktonic foraminifera species (G. ruber (white) and G. truncatulinoides (right)) in core top samples from the Brazilian Continental Margin allowed evaluation of isotopic variability within and between size fractions. Comparison of measured δ18O and δ13C values with predicted modern seawater δ18OEQ and δ13CDIC values allowed estimation of the calcification depth and of δ13C offsets, respectively, for each test size fraction for both species.

Within a single size fraction, maximum variability between replicates using 4-6 tests of G. ruber (white) per analysis for δ18O and δ13C indicates that the use of a larger amount of tests per isotopic analysis will improve accuracy when searching for within-size fraction average population values.

Considering G. ruber (white), lack of significant δ18O differences between sieve size fractions suggests that this species calcify within a similar depth range during ontogeny. The difference between estimated calcification depth (ca. 100 m) and G. ruber mixed layer habitat depth (ca. 50 m) must be taken into account for paleoceanographic interpretations. Regarding δ13C values, a significant increment with sieve size fraction reflected the influence of physiological effects during fractionation and indicates the importance of limiting the sieve size fraction in paleoceanographic studies. The highest sieve size fractions (300-355µm and >355µm) better reflect δ13CDIC values of surface waters in the region and thus are more suitable for reconstruction of ancient surface water nutrient conditions.

Regarding G. truncatulinoides (right), the δ18O increment with sieve size fraction reflected the vertical migration of this species along thermocline waters with calcification of juvenile tests in shallower waters (ca. 250 m) and adult tests in deeper cooler waters (ca. 400 m). δ13C measured values also increased with sieve size fraction, contrasting with the vertical seawater δ13CDIC gradient. Variation in δ13C offsets of G. truncatulinoides (right) suggests that caution must be taken when using δ13C measured in this species for paleoceanographic interpretations.

 

ACKNOWLEDGMENTS

This work was supported financially by the Coordenação de Aperfeiçõamento de Pessoal de Nível Superior (CAPES). We thank Petrobras for providing the samples. The study benefited greatly from the comments of the two anonymous reviewers. We thank Alvar Carranza for his help with the English version of the manuscript.

 

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(Manuscript received 07 August 2010; revised 31 May 2011; accepted 11 June 2011)

 

 

* Corresponding author: paulafrancof@gmail.com