Controls on planktonic foraminifera apparent calcification depths for the northern equatorial Indian Ocean
Stephanie Stainbank aff001; Dick Kroon aff002; Andres Rüggeberg aff001; Jacek Raddatz aff003; Erica S. de Leau aff002; Manlin Zhang aff002; Silvia Spezzaferri aff001
Authors place of work:
Department of Geosciences, University of Fribourg, Fribourg, Switzerland
aff001; School of GeoSciences, Grant Institute, University of Edinburgh, Edinburgh, United Kingdom
aff002; Institute of Geosciences, Goethe University Frankfurt, Frankfurt am Main, Germany
aff003; Frankfurt Isotope and Element Research Center (FIERCE), Goethe University Frankfurt, Frankfurt am Main, Germany
Published in the journal:
PLoS ONE 14(9)
Within the world’s oceans, regionally distinct ecological niches develop due to differences in water temperature, nutrients, food availability, predation and light intensity. This results in differences in the vertical dispersion of planktonic foraminifera on the global scale. Understanding the controls on these modern-day distributions is important when using these organisms for paleoceanographic reconstructions. As such, this study constrains modern depth habitats for the northern equatorial Indian Ocean, for 14 planktonic foraminiferal species (G. ruber, G. elongatus, G. pyramidalis, G. rubescens, T. sacculifer, G. siphonifera, G. glutinata, N. dutertrei, G. bulloides, G. ungulata, P. obliquiloculata, G. menardii, G. hexagonus, G. scitula) using stable isotopic signatures (δ18O and δ13C) and Mg/Ca ratios. We evaluate two aspects of inferred depth habitats: (1) the significance of the apparent calcification depth (ACD) calculation method/equations and (2) regional species-specific ACD controls. Through a comparison with five global, (sub)tropical studies we found the choice of applied equation and δ18Osw significant and an important consideration when comparing with the published literature. The ACDs of the surface mixed layer and thermocline species show a tight clustering between 73–109 m water depth coinciding with the deep chlorophyll maximum (DCM). Furthermore, the ACDs for the sub-thermocline species are positioned relative to secondary peaks in the local primary production. We surmise that food source plays a key role in the relative living depths for the majority of the investigated planktonic foraminifera within this oligotrophic environment of the Maldives and elsewhere in the tropical oceans.
Physical sciences – Chemistry – Chemical properties – Salinity – Physical chemistry – Geochemistry – Earth sciences – Marine and aquatic sciences – Marine environments – Sea water – Oceanography – Water columns – Bodies of water – Oceans – Mineralogy – Minerals – Calcite – Biology and life sciences – Organisms – Eukaryota – Animals – Invertebrates – Plankton – People and places – Geographical locations – Asia – Maldives – Ecology and environmental sciences – Aquatic environments
Planktonic foraminifera are protozoans widely used in paleoceanographic and paleoclimatic studies to interpret and track past marine conditions . They occupy surface to sub-thermocline depths in the pelagic ocean with regional differences in food and seawater properties constraining their latitudinal, temporal and depth distributions. Average living depths (ALD)/Apparent calcification depths (ACD) of foraminiferal species are not globally ubiquitous [2,3]. Thus, accurately constraining regional estimates is important as this bears significance when selecting suitable species for paleoceanographic reconstructions and for interpreting the oceans past vertical thermal structure [4–9].
There are various direct (e.g. concentration profiles calculated from multinet plankton tows, opening-closing nets and sediment traps) and indirect (e.g. test/shell geochemical signatures) methods which can be used to denote foraminifera ALDs and ACDs, respectively. Direct methods allow the sampling of living foraminifera in situ and at a more refined temporal scale yet, are limited by the practicality of refined depth stratified sampling, low abundances, patchiness and inherently incorporate dead or dying foraminiferal tests (shells) from the settling pelagic rain. On the contrary, indirect methods have their own restrictions, as the bulk geochemical signatures are a collated record of the ambient environmental conditions experienced as these micro-organisms migrate within the water column during their life cycle. According to  these organisms have species-specific reproductive depths which are generally associated with the pycnocline. However, as the majority of the calcite is added towards the end of the foraminiferal ontogenetic cycle, adult specimen’s geochemical signatures are generally weighted by the final few precipitated chambers . Furthermore, numerous studies [10–12] have addressed the significant relationship between the geochemical signatures (e.g. δ18O, δ13C, Mg/Ca and Sr/Ca) and size of the planktonic foraminiferal calcitic test. The species-specific size ranges selected for measurement are, therefore, important to take into consideration when conducting such geochemical analyses.
Whether using the δ18O signatures or Mg/Ca ratios from foraminiferal tests to calculate ACDs, a calibrated temperature equation, based on observations from modern oceans, is required. While calibrated for a specific species, size range, region and temperature range, these equations still require additional parameters, which for the paleo-record are often assumed/calculated and, nonetheless, not always available for the present day (i.e. seawater δ18O). Furthermore, compounding factors such as varying cleaning methods (i.e. oxidative with/without reductive cleaning of Mg/Ca samples), post-depositional forces (i.e. diagenesis), species-isotopic offsets, species ecology and lack of regional equations can further influence the calculated estimates [12–15].
Therefore, in this study, we use stable isotopic signatures (δ18O) and Mg/Ca ratios to estimate the inferred depth habitats, here referred to as ACDs, of 14 planktonic foraminiferal species from the Maldives in the northern equatorial Indian Ocean (Table 1). We use our geochemical data collected from core top samples, to assess both stable isotope and Mg/Ca ACD calculation methods and associated published equations. We test and compare the methods of five global studies [12–14,16,17] as they represent (sub)tropical regions, similarly to the present study site, yet have different hydrographic and climatic controls and cover the full range of investigated species (Fig 1).
Consequently, using newly acquired core top data from the Maldives two main hypotheses are tested:
The choice of ACD calculation method can have a significant impact on the final vertical positioning of individual planktonic foraminiferal species.
The ACDs of (sub)tropical planktonic foraminifera are (i) regionally distinct and (ii) controlled by differences in food sources (i.e. position of the deep chlorophyll maximum) linked to thermocline dynamics.
The Asian Monsoon system covers a large region from the western Arabian Sea to East Asia, extending down to North Australia . It is a dynamic climatic system affecting both atmospheric circulation and precipitation. The seasonal reversal in the wind system results in warm, wet continental summers and cool, dry continental winters. These seasonal fluctuations also result in changes in the regional ocean current strengths and directions (Fig 2). Furthermore, regional seasonality in sea surface temperatures (SST), salinity and upwelling occurs. The Asian Monsoon is divided into two subsystems, the South Asian (also known as the Indian) Monsoon (SAM or IM) and the East Asian Monsoon (EAM). The two associated subsystems, roughly divided at a longitude of 105°E, are inherently different due to variations in sea-land distributions . The SAM is the predominant climatic system influencing our study area in the Maldives (Fig 2).
The Maldives archipelago, located south-west of the Indian sub-continent in the northern Indian Ocean, is located within the Arabian Sea. It is a partially drowned carbonate platform, consisting of two rows of North-South orientated atolls bordering an Inner Sea . It sits on a pinnacle, 2000–4000 m, above the adjacent seafloor limiting the maximum depth of the Inner Sea to ~500 m . The SAM-driven winds, northeast and southwest in winter and summer, respectively, drive modern currents in the Maldives (Fig 2). Furthermore, its shallow position results in its intersection with the Oxygen Minimum Zone (OMZ), which regionally extends from ~ 150 m to 1200 m . According to  a local oxygen minimum (~41.017 μmol/kg), generated by wind driven upwelling  is observed at ~ 500 m water depth, this is similar to regional Conductivity, Temperature and Depth probe (CTD) data recorded marginally south of the Maldives by , (Fig 3).
According to , temperature stratification is present across the entire Inner Sea. The surface mixed layer (SML) extends down to 60–70 m and has a temperature range between 28 and 29°C [24,26,27]. The fluorescence profile shows that a deep chlorophyll maximum (DCM), peak in primary production, is present at the base of the SML with a primary peak (F1) at ~69 m water depth with two secondary peaks (F2 and F3) extending from ~80–175 m (Fig 3; [24,26,27]). A sharp thermocline is present at ~70–120 m water depth with temperatures decreasing rapidly across the thermocline down to ~10.21°C at 500 m (Fig 3). Limited seasonal differences occur in the temperature profiles. On the contrary, the seasonal salinity profiles show marked differences, which for the most part are restricted to the SML with the maximum peak at 75–80 m (Fig 3). During the summer southwest monsoon, strong winds generate the eastward flowing Summer Monsoon Current (SMC) from June to October (Fig 2). The reversal in the currents, during the winter northeast monsoon, results in an influx of low salinity water transported from the Bay of Bengal into the southeastern Arabian Sea by the Winter Monsoon Current (WMC) from December to April . As such, the surface winter-summer salinities differ by 0.80 psu, with lower salinities of ~34.10 psu recorded in winter and higher values of ~ 34.90 psu recorded in summer.
Materials and methods
We paired stable isotope (δ18O and δ13C) and select Mg/Ca measurements of 14 planktonic foraminiferal species to calculate their ACDs and infer depth habitat controls (Figs 4 and 5). Planktonic foraminifera live in the upper ~500 m of the ocean  and thus species were selected with previously reported depth habitat preferences to span both shallow and deeper waters (i.e. SML, thermocline and sub-thermocline depths), (Table 1, e.g.: [12,16] and references within). Additionally, a benthic representative made up of two Cibicides species was included in the analyses. This allowed the bottom water temperatures to be constrained and as modern day CTD profiles are available they were used to validate the applied ACD calculation methods for the planktonic foraminifera (i.e. isotopic vs Mg/Ca ACD calculation methods, explained in further detail in the subsequent sections).
Target foraminifera species were isolated from mudline (sediment/water interface) samples (unlithified foraminifera-rich wackestone to packstone, ) of the International Ocean Discovery Program (IODP) Expedition 359, Site U1467 (Fig 2). This site, located at 4°51.0274′N, 73°17.0223′E, was drilled in the middle of the Inner Sea of the Maldives Archipelago at a depth of 487 m  within the drift deposit sediments. The mudline samples are deemed modern as portions were stained onboard with Rose Bengal (1 g/L) which verified the presence of living ostracods as well as benthic foraminifera . Samples were air dried, weighed and washed through a 32 μm sieve. After which, they were dried in an oven for 48 hours at 30°C, weighed and dry sieved into discrete fractions for picking (Table 1). All species were picked from restricted size ranges (Table 1). Appropriate species-specific size ranges were selected, based on the published literature (e.g. [10,12,31], in order to limit intra-specific ontogenetic isotopic fractionation effects. Furthermore, two size ranges were measured for three of the targeted species; G. ruber (w), G. hexagonus and G. scitula to evaluate (pre)adult versus juvenile depth preferences. With two recognised morphotypes of G. siphonifera, we strictly picked the large evolute forms conforming to Type I [1,32] for the geochemical analyses. For all species only pristine ‘glassy’ specimens were picked which had no infilling, discolouration or evidence of reworking (i.e. broken chambers), (Figs 4 and 5).
All 15 species (14 planktonic and 1 benthic, Figs 4 and 5) were analysed for their stable isotopic signatures (δ18O and δ13C) at the Grant Institute of the University of Edinburgh on a Thermo Electron Delta+ Advantage mass spectrometer integrated with a Kiel carbonate III automated extraction line (Table 1). For the isotopic analysis, only C. mabahethi was used as the benthic representative (Fig 5). Two to three replicates were measured for each species, with the exception of C. mabahethi due to the rarity of the species. Prior to analysis, all samples were precleaned by high-powered ultrasonication in Milli-Q water for a few seconds to remove any contaminating phases. The number of specimens analysed varied according to the species and size fraction used, however, in all instances 0.05 mg was required for the analyses (Table 1). The laboratories internal standard was used to calibrate the measurements, which are expressed as parts per mil (‰) relative to VPBD. Replicate measurements give the instrument an analytical precision of 0.1 ‰ for δ18O and δ13C.
Corresponding Mg/Ca ratios were also measured in tests of seven of the species, over the same size fractions used for the stable isotopic analyses (Table 1). Not all species could be analysed, due to the larger sample size needed for these measurements (±25 specimens), compounded by the low abundances of the rarer species and species-specific target size fraction restrictions. Additionally, replicate measurements were only feasible for four of the target species and due to the limited number of benthic specimens in the mudline sample, C. mabahethi and C. wuellerstorfi were combined to obtain Mg/Ca ratios representative of the Inner Sea bottom waters. Prior to measurements, samples were ultrasonically (high-power) cleaned for a few seconds in Milli-Q water. This removed any adhering phases that could introduce sources of carbonate contamination. Subsequently, all samples were cleaned according to the standard oxidative protocol of  with the exclusion of the reductive cleaning step due to the small sample sizes .
Briefly, samples were cracked (the foraminiferal tests were broken open) and rinsed three times in methanol and Milli-Q water in order to remove adherent clay particles. Next, samples were leached with a very weak 0.001N HNO3 acid solution prior to dissolving samples in 0.075M HNO3. Analyses were conducted at the Institute of Geosciences of the Goethe-University of Frankfurt by inductively coupled plasma optical emission spectrometry (ICP-OES) Thermoscientific iCap 6300 (dual viewing). The final centrifuged sample solution was diluted with yttrium water (1 mg/l) prior to measurement in order to correct for matrix effects during ICP-OES analyses. Element/Ca measurements were drift-corrected and standardized using an internal consistency standard (ECRM 752–1, 3.761 mmol/mol Mg/Ca, ). The reproducibility of the ECRM was ~ 0.1 mmol/mol (2 SD). Furthermore, blanks were routinely run to monitor potential contamination during the cleaning process. During all Mg/Ca measurements the elements Al, Fe, and Mn were screened to check for Mn-Fe oxide coatings and clay mineral contamination.
As replicates were measured for the geochemical data (stable isotopes and Mg/Ca), averages were calculated for all species and used in all subsequent calculations (see results section for the raw geochemical data).
Apparent calcification depths (ACDs)
In the literature, authors use either one or a combination of isotope or Mg/Ca methods to calculate their foraminifera ACDs. Each method involves user discretion in the selection of available equations and select variables, thus unavoidably a degree of uncertainty is incorporated into the calculated ACDs. We chose five global, low-latitude, studies from different ocean basins to test their choice of method (Method one: isotope ACD calculations and Method two: Mg/Ca ACD calculations) and equations on our dataset [12–14,16,17]. By using this integrated approach, we were able to assess the accuracy of our estimates as well as comment on the strengths and limitations of each method/equation, in order to select the most appropriate to apply in our study. In all instances, the benthic representative was used as a control to constrain the most applicable equations/approach.
Method one: Foraminifera calcite δ18O (hereafter referred to as δ18Oc) was utilized in two different ways (Method 1.1 and 1.2) to calculate isotope derived ACDs (hereafter referred to as isotope-ACDs). Firstly, in Method 1.1 sea water temperatures were calculated using measured δ18Oc values, an assumed seawater δ18O (hereafter referred to as δ18Osw) value and published δ18Oc-temperature equations. ACDs were then assigned with reference to modern CTD temperature profiles  (Table 2, Fig 3). On the contrary, Method 1.2 involved rearranging published δ18Oc-temperature equations, inserting δ18Osw depth profile data and modern CTD temperature data to calculate the δ18O equilibrium (hereafter referred to as δ18Oe) depth profile. The depths at which the measured δ18Oc values matched the δ18Oe were allocated as the ACDs [13,14,16,17], (Table 2). Method 1.1 and 1.2 are very similar; however, the most notable difference is the δ18Osw allocations. The former method utilizes either just a single δ18Osw value for all species (as is commonly done in the literature) or a combination of different values depending on the assumed species living depth (in this study a broad classification of shallow-/intermediate- versus deep-dwellers was used). On the contrary, the latter method uses a complete δ18Osw depth profile to calculate incrementally the δ18Oe values. As the δ18Osw allocation is essential in the δ18Oc-temperature equations, this distinction is important and justifies the testing of both Methods 1.1 and 1.2.
Method two: Measured foraminifera Mg/Ca ratios were used to calculate Mg/Ca derived ACDs (hereafter referred to as Mg/Ca-ACDs). Seawater temperatures were calculated using the Mg/Ca ratios and published species-specific Mg/Ca-temperature equations. ACDs were then assigned with reference to the modern CTD temperature profiles ([13,17]; Table 2, Fig 3).
Method one: Isotope-ACD calculation methods
A database of species-specific δ18O-temperature equations, for the investigated species, was compiled (S1 Table). Four factors were noted for each, including size fraction measured, sample type, geographical location and temperature calibration range. The equations with factors most comparable to our study and study site were selected (S1 Table). It should be noted that species-specific equations were unfortunately not available for all the investigated species.
 noted only small differences between calibrations, thus in addition to the application of species-specific equations (similarly to ); we tested the implications of using a single equation for all investigated planktonic species. Thus, similarly to the studies of , ,  and  the Globigerinoides sacculifer (now known as Trilobatus sacculifer ) temperature Eq 1 of , the multi-species foraminifera Eq 2 of , the inorganic calcite Eq 3 of  and the synthetic calcite Eq 4 of  were utilized for all species.
In all instances, the δ18Osw values were converted from the VSMOW to VPBD scale by subtracting a suitable correction relative to each equation [41–44].
For Method 1.1, the foraminiferal δ18Oc values were measured, therefore, the only missing and thus assumed variable for these equations was the δ18Osw. We, therefore used δ18O-temperature Eqs 1–4 in addition to species-specific equations in two consecutive calculations to assess the influence of the assigned δ18Osw value.
Firstly, an average δ18Osw value of 0.39 ‰ was used for all equations. This was based on in situ measured seawater values from 0 m and ±500 m from the Maldives region [45–48]. All calculations were then repeated using regionally calculated δ18Osw vertical profiles. Regional δ18Osw depth profiles were calculated by rearranging calibrated salinity equations. The salinity Eq 5 of , Eq 6 of  and Eq 7 of  were calibrated for the study region and thus all were initially tested. Due to seasonal differences, in predominantly the SML, salinity CTD profiles from both summer  and winter  were used in the calculations. Ultimately, published regional δ18Osw values for the surface 0 m [45–47] and ±500 m depth  and the gridded data set of  were used as controls, to select the most suitable equation for the generation of the regional δ18Osw depth profile. Subsequently, average δ18Osw values for 0–75 m (i.e. 75 m coincides with the salinity maximum) and 75–500 m were calculated and used with the δ18O-temperature equations for the reported shallow-intermediate and deeper-dwelling species, respectively (Table 1).
All calculated temperatures were correlated with the modern-day seasonal (summer and winter) CTD profiles and the corresponding depths assigned as the isotope-ACDs. The local temperature profiles of [24,26,27] were all used to account for seasonal variability and as such the final designated isotope-ACDs are averages of the summer and winter calculations.
For Method 1.2, δ18Oc is assumed to have precipitated in equilibrium with the seawater. The seasonal δ18Oe vertical profiles were then calculated by rearranging δ18O-temperature species-specific equations in addition to Eqs 1–4. All equations were used together with the seasonally calculated δ18Osw vertical profiles, obtained using seasonal salinity data [26,27]. The measured planktonic foraminiferal δ18Oc values were compared with the δ18Oe profiles to infer their isotope-ACDs and an overall average from the summer and winter data calculated to assign the respective isotope-ACDs.
Method two: Mg/Ca-ACD calculation method
A database of published Mg/Ca-temperature equations was compiled for all investigated species (S2 Table) with five main factors noted for each (i.e. size fraction measured, sample type, geographical location, temperature calibration range and cleaning method used). The nature of the exponential function combined with the range in associated factors can result in widespread calculated temperatures for each species. Additionally, due to reasons explained in the methods section above, Mg/Ca ratios were only measured for seven of the target species. Consequently, this approach was not used as a principal ACD calculation method but instead to validate the assigned isotope-ACDs.
For all species, there are numerous published equations. To more objectively select the most appropriate species-specific equations for our study location, the following steps were taken:
Equations calibrated using reductively cleaned individuals were treated with caution as several authors [33,52,53] have shown this step reduces the Mg/Ca ratios of both planktonic and benthic species.  reported the reductive treatment resulted in a 10–15% reduction in the Mg/Ca for planktonic foraminifera whereas  reported a reduction of 0.2 mmol/mol for the benthic Cibici(doi)des.
An upper temperature limit of 29.17 ± 0.16°C at 0 m water depth, obtained from local CTD data sets [24,27], was set for our study site. All equations, for the planktonic species, which yielded calculated temperatures above this value were excluded.
A lower temperature limit for the depth at the study site (i.e. 487 m) was set at 10.27 ± 0.17°C, obtained from multiple local CTD datasets [24,26,27]. All equations, for the benthic species which yielded calculated temperatures >1°C either side of this limit were excluded. This limit was arbitrarily set, as due to the steep slope of the CTD temperature profile at this depth a ±1°C restriction sets a depth boundary of ± 100 m.
Again, seasonal (summer and winter) CTD data was used to assign depths to the calculated temperatures with an overall average taken to define the Mg/Ca-ACD values.
Results and discussion
The sedimentary record is an accumulation of foraminiferal tests, which can be from different seasons and represent different stages of their ontogeny as foraminifera migrate through the water column throughout their life cycles recording different geochemical signatures . Thus, as anticipated, replicates of all species show some variability for both δ18Oc and δ13Cc. The mean isotopic values with standard deviations (SD) illustrated in Fig 6, show the 14 planktonic species roughly plot in the expected (as per reports in the literature, e.g. [12,16,17]) vertical order with respect to their δ18Oc signatures (Table 3). The δ13C values of three surface dwelling species (G. glutinata (w/b), G. bulloides and G. rubescens (p)) are depleted, whereas symbiont enrichment is evident in the five symbiont-bearing species (G. ruber (w), G. pyramidalis, G. elongatus, T. sacculifer (w/s) and G. siphonifera). The δ18Oc signatures of the larger G. ruber (w) specimens (355–400 μm) are marginally lower than the smaller specimens (Δ = -0.22 ‰), yet the δ13Cc values are higher for the former (Δ = 0.58 ‰). The smaller G. scitula specimens (125–150 μm) have a lower δ18Oc value, and thus are interpreted to sit shallower in the water column compared with the pre-adult size (180–212 μm) with a more positive value (Δ = 0.42 ‰). A similar disparity (Δ = 0.80 ‰) is noted for their δ13Cc values. On the contrary, the small and large specimens of G. hexagonus display near identical δ13C values, yet a large range in δ18Oc values occurs with overlap of the signatures of the smaller and larger specimens. The benthic species, C. mabahethi, has the highest δ18Oc and lowest Mg/Ca values of 1.43 ‰ and 3.28 mmol/mol, respectively. Whereas, the symbiont bearing G. ruber (w, 355–400 μm) and non-symbiont bearing G. bulloides have the most depleted δ18Oc signature of -2.63±0.12 ‰ and highest Mg/Ca ratio of 7.41 mmol/mol, respectively.
The salinity Eqs 5, 6 and 7 of ,  and  all produce vertical seasonal δ18Osw profiles, which visually look identical, yet the absolute values are significantly offset (Fig 7). Measured in situ regional δ18Osw values for the surface (0 m) by [45–47], at 50 m by  and at ±500 m by  were used to select the most applicable equation for the study site.
Eq 5 of  calculates summer and winter profiles with positive surface values with an average of 0.42 ‰ which is comparable to the in situ measurements. On the contrary the bottom water δ18Osw is over estimated (average at 500 m = 0.59 ‰) and is out of the local range measured by , (Fig 7). The Eq 6 of  produces summer and winter profiles with negative values for the top 50 m of the water column with average values of -0.33 ‰ and 0.01 ‰ at the surface and 500 m water depth, respectively. Overall, the profiles have significantly lower values in comparison to the in situ data. On the contrary, all calculated values are positive using the Eq 7 of  with average values of 0.35 ‰ and 0.40 ‰ at the surface and 500 m water depth, respectively. The latter equation calculates δ18Osw values comparable to the measured regional surface δ18Osw data of [45–47], with a range of δ18Osw from 0.32 to 0.74 ‰, and an average δ18Osw = 0.49 ‰. They were also comparable to the regional δ18Osw values measured at ±500 m water depth by  with a range of δ18Osw from 0.26 to 0.42 ‰, and an average δ18Osw = 0.30 ‰.
The calculated δ18Osw profiles are also compared with the gridded dataset of  from the Maldives region (Fig 7). The Eq 7 of  derived values are most similar with the gridded dataset. These calculated profiles have slightly lower values than the gridded dataset for the top 80 m and marginally higher values down to 500 m. There is, however, a lack of measured subsurface δ18Osw data from the northern Indian Ocean. The low spatial and depth resolution of the subsurface data significantly limits the interpretation and application of the gridded dataset and thus we used this dataset solely to verify the calculated profiles.
Overall, all equations underestimate the δ18Osw at 50 m with none of the calculated profiles having values corresponding to the measured value by  at 50 m. Nevertheless, considering its correlation with the in situ surface and bottom water δ18Osw, the salinity Eq 7 of  is deemed most suitable for this study. The δ18Osw average for the SML down to a depth of 75 m, coinciding with the maximum salinities, is 0.38 ‰ with an average of 0.40 ‰ for 75–500 m water depth. The winter and summer averages for the same ranges are 0.36 ‰, 0.40 ‰ and 0.39 ‰, 0.40 ‰, respectively.
Method one: Isotope-ACD estimates
As stated above, Method one tests the applicability of using individual species-specific δ18O-temperature equations (e.g. , , , , ) versus applying Eqs 1–4 for all species as well as different δ18Osw values in two separate applications: Method 1.1 and 1.2.
Method 1.1: δ18O-temperature and isotope-ACD allocations
In Method 1.1 when using a single δ18Osw value of 0.39 ‰ (Table 4), allocated based on an average of published values for 0 m and ±500 m from the Maldives region [45–48], Eqs 1, 3 and 4 calculate high temperatures and thus result in shallower ACD allocations for all assumed shallow-dwelling species (Table 1) in comparison to Eq 2. Additionally, calculated temperatures, for G. ruber (w, 355–400 μm), G. rubescens (p) and G. bulloides are above the local CTD measurements for Eqs 1 and 4 and as such have no assigned ACDs. When assessing the first four species (G. ruber (w), T. sacculifer, N. dutertrei and G. bulloides) with calibrated species-specific equations (, , ), Eqs 1, 3 and 4 derived ACDs are considerably shallower than the species-specific and Eq 2 ACD allocations. The largest differences are noted for G. ruber (355–400 μm) and G. bulloides.
On the contrary, the species-specific derived ACDs for the intermediate dwellers P. obliquiloculata and G. menardii are not as cohesive with Eq 2. The assigned ACD, using the species-specific equation of , for the former species is more comparable to the inferred ACDs from Eqs 1, 3 and 4 than to Eq 2. However, as the P. obliquiloculata species-specific equation from  is based on modelled data which shows a large spread and relatively low correlation, we still consider Eq 2 as most suitable for use in accordance with the other shallow to intermediate-dwellers. Furthermore, both Eqs 2 and 3 result in assigned ACDs comparable to the species-specific allocation for G. menardii, however, similarly to above, we still consider the former most applicable for use with this intermediate-dwelling species.
The benthic allocation from Eq 3 (497±16 m) is directly comparable to the study site depth of 487 m. It is apparent though that the allocated δ18Osw is possibly marginally too low for use with the deeper-dwelling sub-thermocline species, as the species-specific benthic equation of  produced a deeper ACD estimate (533±10 m) than the study site. On the contrary, Eqs 1 and 4 benthic ACD allocations are significantly shallower, with the Eq 2 estimates exceedingly deep and as such these Eqs. do not appear suitable for application with the deeper-dwelling sub-thermocline species. In this instance, however, a higher δ18Osw value could offset the use of an equation calibrated for a SML species.
Calculations were then repeated for Method 1.1, using the calculated δ18Osw values obtained using the salinity Eq 7 of  (Table 5). A δ18Osw value of 0.38 ‰, averaged for the top 75 m water depth, is used for the reported shallow (SML) and intermediate- (thermocline) dwelling species. Whereas, a δ18Osw value of 0.40 ‰, averaged for 75–500 m water depth, is used for the reported deeper-dwelling (thermocline to sub-thermocline) species. The delineation at 75 m was assigned based on the salinity maxima from local CTD data (Fig 3; [26,27]).
The allocation of marginally different δ18Osw values for the SML and deeper depths results in slight differences in temperature calculations and subsequent ACD assignments. As the δ18Osw value for the surface and sub-surface depths is similar to the first calculations, minimal differences in ACDs are noted for these shallow to intermediate-dwelling species. Eq 2 derived ACDs are still most comparable with those allocated using the species-specific equations, with again the exception of P. obliquiloculata. Additionally, ACDs allocated using Eqs 1, 3 and 4 have estimates which are again significantly shallower. On the contrary, as noted above, using a higher δ18Osw value for the thermocline and sub-thermocline species results in shallower benthic ACD estimates. In particular, the benthic ACD estimate when using Eq 3 (496±10 m) is again most comparable to the study site with the species-specific equation providing a slightly deeper ACD estimate of 527±5 m. We use the equation of , calibrated for the genera Cibicidoides and Planulina, for our benthic species, C. mabahethi. It is assumed that both the Cibicidoides and Planulina genera calcify in near equilibrium to the surrounding seawater. It is, however, questionable whether all benthic species precipitate in isotopic equilibrium with the seawater. Thus, when applying the equation of , small differences between the Cibicidoides and Planulina genera and the investigated species, C. mabahethi could account for these deeper ACD estimates. Furthermore, our utilized δ18Osw value of 0.40‰ could still be too low, especially considering  measured a range in δ18Osw values (0.26–0.42 ‰) within the Maldives Inner Sea.
Therefore, we conclude that, if using a single δ18Osw value or an averaged value for the SML and thermocline to sub-thermocline waters, it is plausible to use Eq 2 of  for surmised shallow to intermediate-dwelling species and Eq 3 of  for all other deeper-dwelling (thermocline to sub-thermocline) species ACD calculations as applied in . Applying only species-specific equations would still be the preferred method yet, as they are not always available, their use to crosscheck and validate a chosen single equation to utilize for all species is advised.
It should be noted that care must be taken when allocating the δ18Osw values for use in the δ18O-temperature equations. In this particular instance if only in situ shallow water (0–50 m) measurements are taken into consideration, averages of 0.58–0.70 ‰ would be obtained. The deeper water salinity maximum would skew the data and using a considerably higher δ18Osw allocation, in the calculations, would result in significantly different ACD estimates. In this instance, we took an average from the surface (0 m) and bottom (±500 m) water measurements, which avoids unintentionally over estimating the δ18Osw value.
Method 1.2: δ18Oe profiles and isotope-ACD allocations
For Method 1.2, seasonal δ18Osw profiles, calculated using the salinity Eq 7 of , are used together with Eqs 1–4 in order to generate vertical δ18Oe profiles (Fig 8). Eq 2 calculates the lowest δ18Oe values for the top ±80 m with the surface waters being 0.62–0.72 ‰ lower than the values derived when using Eqs 1, 3 and 4. The latter three δ18Oe profiles are comparable down to ~120 m, after which the Eq 3 derived graph is consistently lower and Eq 4 has the highest values, yet only marginally in comparison to Eq 1.
ACDs are subsequently allocated using the seasonal vertical δ18Oe profiles produced in Fig 8. In addition, as conducted by  selected species-specific equations are used to further assess the applicability of the other four equations (Table 6). As expected, when using the Eqs 1, 3 and 4 derived graphs, the shallow to intermediate-dwelling species have the shallowest ACDs, which are consistently shallower in comparison with the species-specific allocations. On the contrary, ACDs assigned using the Eq 2 derived graph, are nearly identical with the allocated ACD values for the four shallow-dwelling species with species-specific equations (G. ruber, T. sacculifer, N. dutertrei and G. bulloides). Species-specific equations are available for two deeper, thermocline species (P. obliquiloculata and G. menardii) and for the former the derived ACDs are on the contrary more comparable with those derived from Eqs 1, 3 and 4. Yet, similarly to above, this species is anomalous as the species-specific equation was obtained from modelled data and as such, we chose to allocate Eq 2 as most applicable.
Finally, the benthic ACD allocations vary significantly when comparing all five estimates. As the study site depth is shallow, and known at 487 m, it is apparent that the benthic estimate using Eq 3 is most comparable. ACDs derived using Eqs 1 and 4 are considerably shallower whereas a significantly deeper ACD is assigned when using the δ18Oe profile from Eq 2. The Cibicidoides and Planulina equation of  estimates an ACD of 528±5 m, which again is deeper than the known depth of the study site.
Similarly, to Method 1.1, the best approach to derive δ18Oe values is to use species-specific equations. However, as these are not always available for all investigated species a single equation is required for use with multiple species. Overall, we conclude that Eqs 2 and 3 of  and  are most applicable for our dataset, as previously mentioned when using Eq 1 of  and Eq 4 of  the assigned ACDs are all consistently too shallow. Thus, based on their agreement with the species-specific derived ACDs and benthic allocations, and similarly to Method 1.1, we found it suitable to use Eq 2 for the shallow to intermediate-dwelling (SML-thermocline) species and Eq 3 for the deeper-dwelling (thermocline to sub-thermocline) species. Alternatively, Eq 3 could be applied for all species yet there is the possibility of slightly shallower ACD estimates for the SML dwelling species.
Method two: Mg/Ca-ACD estimates
There is a large spread in the temperature estimates from the applied species-specific equations (Fig 9). As previously mentioned, this was anticipated due to the large variability in the calibration parameters (e.g. geographical location, temperature calibration range, specimen cleaning method) and the quadratic nature of the Mg/Ca-temperature equations. The choice of applicable equation is significant as the subsequent ACDs can be quite offset. Suitable species-specific Mg/Ca-temperature equations were, therefore, firstly constrained using the steps outlined in the Methods section above (Fig 9). Following this, all factors were assessed to select the species-specific equations most suitable for our study and study site (Fig 9). The subsequent Mg/Ca-ACD allocations are somewhat comparable to the isotope-ACDs (Table 7). Some disparity was anticipated between the two methods, as the isotopic data incorporates a salinity effect and were additionally not corrected for species-specific isotopic offsets.
The Mg/Ca-ACDs for all species, except G. bulloides, are shallower than their isotope-ACD counterparts. This could be attributable to the natural geochemical variability incurred through the measurement of different specimens. Additionally, a possible salinity influence for the surface dwellers G. ruber (w), T. sacculifer (w/s) and G. siphonifera could account for the marginal Mg/Ca- and isotope-ACD differences ranging between 7–20 m. Globigerina bulloides has comparable Mg/Ca- and isotope-ACD estimates. Yet for the deeper dwellers, P. obliquiloculata and G. menardii the isotope- and Mg-/Ca-ACDs vary significantly. In this instance, we attribute the differences not to hydrological conditions but instead to the applied equations and species morphology. Particularly for these two species, there are few species-specific calibrated equations and as such, we are limited in the choice of equations to apply. Furthermore, both species precipitate secondary calcite, for G. menardii as an encrusted keel and for P. obliquiloculata in the form of a cortex. As such, using variable specimens for the respective geochemical analyses would result in further variability in the geochemistry and subsequently their inferred ACDs. This is particularly evident in the variation of the G. menardii replicates. As the measurements for this species were highly variable, in comparison to the other replicate datasets, we did not calculate an average but instead treated each replicate separately. The resultant ACDs range from 70–90 m, which, even though are still shallower than the isotope-ACD allocation, reflect the natural variation within the species.
We further attribute the difference in isotope-ACD and Mg/Ca-ACD allocations for P. obliquiloculata to the differential Mg/Ca distributions between the species inner test and outer cortex layer. Using Laser–ablation inductively coupled plasma–mass spectrometry (LA-ICP-MS),  showed the cortex Mg/Ca values are around 3–10 times lower in comparison to the inner test geochemistry. Furthermore, the cortex thickness was shown to be variable and as such, its influence on bulk geochemistry measurements would vary. Therefore, as a consequence of using different species for the isotopic and geochemical measurements in this study, in conjunction with having to pool multiple specimens for the various measurements could account for these different ACD allocations for P. obliquiloculata.
Planktonic foraminifera ACD allocations
Regionally distinct ecological niches develop due to differences in water temperature, nutrients, food availability, predation and light intensity all of which contribute to the vertical dispersion of planktonic foraminifera. Understanding these distributions is thus important for regional paleoceanographic reconstructions (e.g. [2,17]). Important to consider is planktonic foraminifera living depths are not globally ubiquitous [2,3]. This can be due to differing quality and quantity of available prey, different genotypes  or hydrographic variability. Additionally, ACD calculation methods and sampling strategies differ across authors, such as sampling at different times during species ontogenic cycles or targeting different species-specific size ranges. These can all incorporate further discrepancies into the foraminifera ACD estimates that are demonstrated in the comparison of Fig 10.
The five global, low latitude ACD studies referenced in this work (i.e. studies A-E [12–15,17], Fig 1), were selected as they have different regional hydrological controls, and used different methods and equations to calculate their foraminiferal ACD estimates. In addition, 12 common species were analysed yet were from variable size fractions reflecting different instances during each species ontogenetic cycles (Fig 10). It is, therefore, difficult to disentangle all contributions accounting for these observed ACD differences, however, as this study tested all authors’ methods and equations, some comment can still be made.
The first four studies [12–14,16] calculated isotope-ACDs, each utilizing a different combination of equations and δ18Osw values. The largest deviations are noted for the surface-dwelling species, G. ruber (w), G. rubescens (p), T. sacculifer (w/s) and G. glutinata (w/b) which can in part be attributed to equation selection, thermocline depth differences and specimen selection (Fig 10). Studies A  and D  both have shallower SMLs (30–40 m). Additionally, they utilized Eqs 1 and 4 for all ACD calculations, which we found produced considerably shallower ACDs. Therefore, equation choice in conjunction with more condensed SMLs could account for the observed deviations. Additionally, we exclusively used T. sacculifer which displayed gametogenic features (i.e. a sac like final chamber) and G. glutinata specimens with bulla, which were recognized by [29,80,81] as possible reproductive structures. These species are known to migrate to deeper waters towards the end of their ontogenetic cycle, which is reflected in this study with comparably deeper ACDs for these two species.
On the contrary, in comparison with the present study, both studies B  and C  have comparable SML depths. The latter applied species-specific equations, however, used relatively large size ranges for each species, which could contribute to the large range and differences in the shallow-dwelling species ACDs. Study B of  calculated foraminifera ACDs for samples from three distinct regions in the Caribbean, east Atlantic Ocean and west Atlantic Ocean. Our thermocline structure is most similar to the latter region and thus for simplicity we only displayed these ACDs in the comparison of Fig 10.  used comparable size fractions, yet utilized Eq 4, which as expected results in marginally shallower ACDs estimates. For both G. ruber (w) and T. sacculifer calculations, they did report Eq 2 derived ACDs, which are accordingly slightly deeper and more comparable with our inferred depths (Fig 10).  reported deep shoaling (i.e. congregating) observations for some planktonic foraminifera in the subtropical eastern North Atlantic. This was attributed to subsequent deepening of the SML in summer (100–150 m) and association with increasing temperatures. The low latitudinal position of the Maldives, together with increased light and higher SST temperatures could support a deeper depth habitat of the surface dwellers in the tropical, Indian Ocean.
Globigerinella siphonifera and G. ungulata have comparable ACDs across the first four studies as do the typically thermocline and sub-thermocline dwelling N. dutertrei, P. obliquiloculata (w/c), G. menardii, G. hexagonus and G. scitula (Fig 10; [12–15]. The opportunistic species, G. bulloides shows a large spread (Fig 10); this is probably a combination of differences in calculation methods as well as a reflection of its wide-ranging depth habitat preferences as a result of differential seasonal upwelling conditions across the study locations.
The final isotope-ACD calculation method we selected was similar to that applied in study E of , albeit their final ACDs are derived from a combination of isotope- and Mg/Ca methods. In addition, they analysed specimens from a large size range, in contrast to the restricted size fractions used in this study. Both shallow-dwelling species, G. ruber (w) and T. sacculifer (w/s) have overlapping ACD ranges whereas deviations for N. dutertrei, P. obliquiloquilata (w/c) and G. hexagonus ACD allocations are apparent. Regional differences in thermocline and nutrient conditions can account for these differences. In the present study, the SML is shallower extending down to ~69 m water depth with a thermocline between ~70–120 m. On the contrary,  reported a SML extending down to 105 m and a thermocline between 130–230 m water depth in the West Pacific Warm Pool (WPWP) which could account for the deeper living depths for all species from study E.
Northern equatorial Indian Ocean ACD controls
This study attempts to constrain foraminiferal ACDs for the northern equatorial Indian Ocean using a combination of stable isotopes and Mg/Ca ratios (explained in the sections above). Previous studies (e.g. [1,3]) have reported that the vertical peak in planktonic foraminifera standing stocks is linked to the DCM. Thus, as hypothesized, this positioning also appears to influence the foraminiferal ACDs at our study location in the Maldives in the northern equatorial Indian Ocean.
All investigated shallow to intermediate-dwelling species congregate at the base of the SML and in the upper thermocline around the DCM peaks F1 and F2 with an average range between 73–109 m depth (Figs 10 and 11). This DCM is generally situated between the upper nutrient-depleted waters and the lower light depths of the euphotic zone in pelagic oceans. Generally, it is associated with a high production and biomass of phytoplankton . As the geochemical signatures are weighted by the final few precipitated chambers, and we can assume that the majority of the adult specimens measured in this study underwent reproduction, particularly in the case of G. ruber (w), G. glutinata (w/b), G. rubescens (p) and T. sacculifer (w/s), the observed concentration around the DCM peaks is justified. The DCM thus not only provides a source of prey for adult/pre-adult foraminifera, but the enhanced survival of juveniles is also supported. Additionally, high temperatures in conjunction with high light levels could force the typical surfacing dwelling foraminifera deeper into the water column.
As a result of the SAM, the northern Indian Ocean and Arabian Sea have a wide range of biogeochemical provinces. The north-western portions of the Arabian Sea have high productivity and upwelling zones whereas our study site in the Maldives, in the eastern edge, is oligotrophic with little or no upwelling . The closest regional analogue to this study is the depth stratified plankton tow research of  from the western Arabian Sea (Study F; Fig 1). With seven species being in common, our calculated ACDs are marginally deeper than their reported ALDs at the non-upwelling stations (Fig 12). These differences could be a result of the geochemical signatures of adult tests being weighted by the final few precipitated chambers, which generally form when they are deeper in the water column, in addition to variations in the vertical structure of the water column. The DCM and SML are positioned shallower in the Western Arabian Sea, between 29–45 m (Fig 12). Furthermore,  found two maxima in test concentrations at their non-upwelling sites, the first was at the surface dominated by juveniles with a second deeper maximum linked with the DCM and represented by adult specimens. This is in accordance with the present study, albeit our DCM sits deeper in the water column in comparison to the study of .
Shallow and intermediate-dwelling species
Symbiont-bearing species have a light dependency; making them more prolific in the tropics and sub-tropics within the SML. Five symbiont-bearing species were included in our study: G. ruber (w), its morphotype G. pyramidalis, G. elongatus, T. sacculifer (w/s) and G. siphonifera. Furthermore, three additional shallow-dwelling species were analysed G. glutinata (w/b), G. rubescens (p) and N. dutertrei. According to [1,2] both G. glutinata (w/b) and N. dutertrei have been found to facultatively host algal symbionts, whereas, G. rubescens (p) could possibly host symbionts, based on its phylogenetic placement.
All typical SML species ( and references within) have shallow ACDs ranging between 74–92 m reflecting their affinity for the photic zone. The shallowest dwellers in this group are the larger G. ruber specimens and G. rubescens (p), (both isotope-ACDs = 74±2 m) with the deepest dweller being G. siphonifera (isotope ACD = 92±4 m).
 recognized the close link between G. ruber (w) and T. sacculifer (w/s) and the DCM in oligotrophic waters and as shown here even the symbiont-bearing species appear to utilize it as a food source.  reported T. sacculifer (w/s) having a deeper ACD as opposed to G. ruber in areas with a thick SML, whereas similar depths have been attributed in regions with a shallow SML. Our study, with a shallow local SML, supports this as both G. ruber (w, 212–250 μm), (isotope-ACD = 77±4 m and Mg/Ca ACD = 70±1 m) and T. sacculifer (w/s), (isotope-ACD = 83±7 m and Mg/Ca ACD = 70 m) have over-lapping estimates. The species, G. ruber (w) is generally considered to dwell within the first 30 m of the water column  with a preferable temperature around ±27°C . Although our ACD estimates are deeper, they agree well with this optimal temperature. Furthermore, the G. ruber (w) group is considered to be composed of a number of morphotypes (i.e. G. pyramidalis and G. elongatus or G. ruber sensu stricto and sensu lato) with studies by [85–88] suggesting differing calcification depths for each. Based on the work of , G. elongatus is currently considered a separate species in the modern fauna, as opposed to G. pyramidalis which is still a morphotype of the classical G. ruber (w). Our data shows comparable ACDs for all three with identical isotope-ACDs for G. elongatus and G. pyramidalis of 78±4 m.
Our ACDs conform to other studies identifying T. sacculifer as dwelling within the first 80 m of the water column [16,17]. Furthermore, T. sacculifer has been reported to migrate to deeper depths to reproduce [1,90]. Specimens at the end of their ontogenetic cycle were selected for analysis in this study, based on the assumption that all specimens with a sac have undergone reproduction . Thus, we can assume that our ACD estimates reflect this gametogenic affinity.
With two recognised morphotypes of G. siphonifera [1,32], we strictly picked the large evolute forms conforming to Type I for the geochemical analyses. Both the isotope- and Mg/Ca-ACD estimates, 92±4 m and 72±1 m respectively, position this species deeper in the water column in the upper thermocline. This is in accordance with observations for the Type I morphotype in the Caribbean . While deeper in the water column, it is still within the photic zone and as such, its symbionts can still be supported.
Both G. glutinata (w/b) and G. rubescens (p) are small (<250 μm), ubiquitous species in tropical/subtropical surface waters with large ranges reported in their depth habitats. At the study site G. glutinata (w/b) lives deeper in the upper thermocline at 81±5 m below the DCM peak F1 at the base of the pycnocline (Fig 11). The latter, G. rubescens (p) has a marginally shallower isotope-ACD of 74±2 m and according to past studies [2,29,93,94] its vertical distribution is heavily controlled by nutrient availability. Our isotope-ACD estimate places this species in the upper thermocline within peak F1, which would support the premise of it displaying some light dependency, while still being positioned close to the DCM.
Neogloboquadrina dutertrei has been shown to facultatively host symbionts [2,29], yet similarly to G. bulloides is an opportunistic species . Their depth habitats are thus heavily governed by prey availability and local hydrography and consequently both species are recognized as SML/thermocline dwellers. The former, N. dutertrei has a deeper ACD (isotope-ACD = 97±4 m) than G. bulloides. Globigerina bulloides has the shallowest isotope-ACD estimate of 73±2 m with its Mg/Ca-ACD comparable at 76±4 m. Both these estimates place it within the DCM peak F1, which is surmised to reflect its opportunistic behavior.
Pulleniatina obliquiloculata (w/c) and the globorotalids G. menardii and G. ungulata are considered to be SML to thermocline dwellers with their highest standing stocks linked to the pcynocline/DCM [1,96,97]. Globorotalia ungulata (isotope-ACD = 81±6 m) has an ACD positioned in the upper thermocline whereas both P. obliquiloculata (w/c), (isotope-ACD = 104±6 m; Mg/Ca-ACD = 74±3 m) and G. menardii (isotope-ACD = 109±8 m; Mg/Ca-ACD = 70–90 m) are situated in the lower thermocline. The species P. obliquiloculata (w/c) is known to precipitate gametogenic calcite towards the end of its ontogenetic cycle as it migrates to deeper depths forming a cortex . Specimens used for this study had this smooth layer of pre-gametogenic calcite, thus its ACD is deeper in the upper thermocline close to the DCM peak F2. Similarly, both thermocline-dwelling globorotalids (G. menardii and G. ungulata) are associated with the DCM peak F2 with the latter shallower at the base of the pycnocline.
The deepest dwelling species are G. hexagonus and G. scitula. Globorotalia scitula is cosmopolitan whereas, G. hexagonus is rare and restricted to the Indo-Pacific , however,  have questioned this species spatial restriction. Juvenile and (pre)adult specimens of both species were included in this study to allow some comment on their life strategies. Overall, both were found to co-occur at sub-thermocline depths. These concomitant depth habitats were similarly reported for the central Arabian Sea [1,100]. Both species appear to be associated to and respond to peak F3 in the fluorescence vertical profile (Fig 11) and thus by inference chlorophyll. Thus, similarly to  we associate their depth habitats to food preferences. Considering the oligotrophic study site, these deeper peaks in phytoplankton would likely serve as a food source. Their tolerance for low-oxygen environments is also confirmed as their depths coincide with the most depleted oxygen levels in the top 500 m of the water column (Fig 3).
Differing accounts exist of the environmental tolerances of G. hexagonus.  report it as having a broad tolerance whereas  associate it with restricted environmental preferences. Nevertheless, there is general consensus regarding an association to high nutrient conditions [1,17,101] with  surmising it to be herbivorous in nature. Furthermore,  identified it as an upwelling indicator for the Oligocene and Miocene with  using G. hexagonus δ13C records to reconstruct past eastern equatorial Pacific sub-thermocline water mass contributions. Again, this species nutrient affinity can be confirmed in this study (Fig 11). The smaller juveniles (180–212 μm) have a deeper inferred ACD (isotope-ACD = 218 ± 22 m) in comparison to the pre-adults (isotope-ACD = 163 ± 4 m) with the latter associated to DCM peak F3. This could reflect their surmised reproductive strategy of ascending to shallower depths to reproduce , this difference in vertical positioning is, however, not mirrored in the isotopic data of .
Globorotalia scitula is a medium sized foraminifera (>150 μm) and has been reported in highest abundances during periods of enhanced primary productivity . The smaller juveniles (125–150 μm) have a considerably shallower isotope-ACD of 194±22, within peak F3, in comparison to the larger specimens (180–212 μm) sitting deeper at 277±27 m. This species is also surmised by  to ascend to shallower depths to reproduce. As the adults/pre-adults similarly had higher δ18Oc values in , which would also equate to deeper ACDs in comparison to the juveniles, further comment on this reproductive strategy cannot be made.
While this study is not intended as a review of all foraminiferal ACD calculation methods (isotope and Mg/Ca) and available equations, our comparison does highlight the need to acknowledge these different criteria, in addition to regional hydrological differences, when comparing global studies. Both ACD calculation methods result in variable erroneous values as each requires the selection of suitable equations, the justification of which is not always straightforward. In all instances, the species-specific equations are found to be most robust. However, in their absence a single or paired selection of equations for all species can yield similar results when suitable δ18Osw values are applied particularly for thermocline and sub-thermocline dwelling species. Furthermore, while species-isotopic offsets are inherently incorporated, a correction can be applied to account for these disequilibrium effects. We did not apply any corrections in this study, as they were not available for all investigated species. Additionally, applying different δ18O-temperature equations for all species affects the absolute ACD values yet the relative species-specific vertical ordering remains consistent. This is an important consideration when comparing data with the published literature. Lastly, while the Mg/Ca-ACD calculation method is not used as the primary approach in this study, the ACDs prove comparable, within 30 m, to the isotope-ACD allocations.
Overall, previously reported planktonic foraminiferal ecological affinities are confirmed for the northern equatorial Indian Ocean for the 14 investigated species. Presently, the water column is highly stratified at the study site in the Maldives, with all ACDs of the shallow- and intermediate-dwellers positioned at the base of the SML and along the thermocline between 73–109 m depth. The DCM appears as a primary control for these shallower-dwelling species, with the sub-thermocline species depth habitats possibly linked to secondary peaks in the local primary production. The shallow-dwelling species G. bulloides, G. ruber (w), G. elongatus, G. pyramidalis and G. rubescens (p), are positioned at the base of the SML within the pycnocline within or directly below the DCM peak F1. Whereas, G. glutinata (w/b), G. ungulata and T. sacculifer (w/s) are positioned directly below the pycnocline within the salinity maxima. Conversely, the intermediate-dwelling G. siphonifera, N. dutertrei, P. obliquiloculata (w/c) and G. menardii have inferred ACDs in the lower thermocline. Changes in the apparent responses between these shallow- (e.g. G. ruber and G. glutinata), intermediate- (e.g. N. dutertrei and G. siphonifera) and deeper-dwellers (G. scitula and G. hexagonus) could ultimately be utilized for regional paleoceanographic reconstructions. As such, by using a combination of foraminiferal proxies (i.e. δ18O, δ13C and Mg/Ca) for select species from these different depth habitats; past changes (e.g. temperature, salinity, nutrients, chlorophyll) in upper ocean stratification can be constrained and linked back to SAM intensity, variability and associated upwelling.
S2 Table [docx]
Compilation of species-specific foraminiferal Mg/Ca-temperature equations.
1. Schiebel R, Hemleben C. Planktic Foraminifers in the Modern Ocean. Berlin: Springer-Verlag; 2017
2. Rebotim A, Voelker AHL, Jonkers L, Waniek JJ, Meggers H, Schiebel R, et al. Factors controlling the depth habitat of planktonic foraminifera in the subtropical eastern North Atlantic. Biogeosciences. 2017;14: 827–859. doi: 10.5194/bg-14-827-2017
3. Peeters FJC, Brummer G-JA. The seasonal and vertical distribution of living planktic foraminifera in the NW Arabian Sea. Geol Soc London Spec Publ. 2002;195: 463–497. doi: 10.1144/GSL.SP.2002.195.01.26
4. Ganssen GM, Peeters FJC, Metcalfe B, Anand P, Jung SJA, Kroon D, et al. Quantifying sea surface temperature ranges of the Arabian Sea for the past 20 000 years. Clim Past. 2011;7: 1337–1349. doi: 10.5194/cp-7-1337-2011
5. Anand P, Kroon D, Singh AD, Ganeshram RS, Ganssen G, Elderfield H. Coupled sea surface temperature-seawater δ18O reconstructions in the Arabian Sea at the millennial scale for the last 35 ka. Paleoceanography. 2008;23: PA4207 doi: 10.1029/2007PA001564
6. Ford HL, Ravelo AC, Dekens PS, LaRiviere JP, Wara MW. The evolution of the equatorial thermocline and the early Pliocene El Padre mean state. Geophys Res Lett. 2015;42: 4878–4887. doi: 10.1002/2015GL064215
7. Lynch-Stieglitz J, Polissar PJ, Jacobel AW, Hovan SA, Pockalny RA, Lyle M, et al. Glacial-interglacial changes in central tropical Pacific surface seawater property gradients. Paleoceanogr Paleoclimatology. 2015;30: 423–438. doi: 10.1002/2014PA002746
8. Bunzel D, Schmiedl G, Lindhorst S, Mackensen A, Jesús R, Romahn S, et al. A multi-proxy analysis of Late Quaternary ocean and climate variability for the Maldives, Inner Sea. Clim Past. 2017;13: 1791–1813. doi: 10.5194/cp-13-1791-2017
9. Raddatz J, Nürnberg D, Tiedemann R, Rippert N. Southeastern marginal West Pacific Warm Pool sea-surface and thermocline dynamics during the Pleistocene (2.5–0.5 Ma). Palaeogeogr Palaeoclimatol Palaeoecol. 2017;471: 144–156. doi: 10.1016/j.palaeo.2017.01.024
10. Elderfield H, Vautravers M, Cooper M. The relationship between shell size and Mg/Ca, Sr/Ca, δ18O, and δ13C of species of planktonic foraminifera. Geochemistry, Geophys Geosystems. 2002;3. doi: 10.1029/2001GC000194
11. Friedrich O, Schiebel R, Wilson PA, Weldeab S, Beer CJ, Cooper MJ, et al. Influence of test size, water depth, and ecology on Mg/Ca, Sr/Ca, δ18O and δ13C in nine modern species of planktic foraminifers. Earth Planet Sci Lett. 2012;319–320: 133–145. doi: 10.1016/j.epsl.2011.12.002
12. Birch H, Coxall HK, Pearson PN, Kroon D, O’Regan M. Planktonic foraminifera stable isotopes and water column structure: Disentangling ecological signals. Mar Micropaleontol. 2013;101: 127–145. doi: doi.org/10.1016/j.marmicro.2013.02.002
13. Anand P, Elderfield H, Conte MH. Calibration of Mg/Ca thermometry in planktonic foraminifera from a sediment trap time series. Paleoceanography. 2003;18: 1050. doi: 10.1029/2002PA000846
14. Mohtadi M, Oppo DW, Lückge A, DePol-Holz R, Steinke S, Groeneveld J, et al. Reconstructing the thermal structure of the upper ocean: Insights from planktic foraminifera shell chemistry and alkenones in modern sediments of the tropical eastern Indian Ocean. Paleoceanography. 2011;26: PA3219. doi: 10.1029/2011PA002132
15. Farmer CE, Kaplan A, de Menocal PB, Lynch-Stieglitz J. Corroborating ecological depth preferences of planktonic foraminifera in the tropical Atlantic with the stable oxygen isotope ratios of core top specimens. Paleoceanography. 2007;22: PA3205. doi: 10.1029/2006PA001361
16. Steph S, Regenberg M, Tiedemann R, Mulitza S, Nürnberg D. Stable isotopes of planktonic foraminifera from tropical Atlantic/Caribbean core-tops: Implications for reconstructing upper ocean stratification. Mar Micropaleontol. 2009;71: 1–19. doi: 10.1016/j.marmicro.2008.12.004
17. Rippert N, Nürnberg D, Raddatz J, Maier E, Hathorne E, Bijma J, et al. Constraining foraminiferal calcification depths in the western Pacific warm pool. Mar Micropaleontol. 2016;128: 14–27. doi: 10.1016/j.marmicro.2016.08.004
18. Schlitzer R. Ocean Data View. 2018. Available: odv.awi.de
19. Wang P, Clemens S, Beaufort L, Braconnot P, Ganssen G, Jian Z, et al. Evolution and variability of the Asian monsoon system: state of the art and outstanding issues. Quat Sci Rev. 2005;24: 595–629. doi: 10.1016/j.quascirev.2004.10.002
20. Spezzaferri S, El Kateb A, Pisapia C, Hallock P. In situ observations of foraminiferal bleaching in the Maldives, Indian Ocean. J Foraminifer Res. 2018;48: 75–84.
21. Betzler C, Hübscher C, Lindhorst S, Reijmer JJGG, Römer M, Droxler AW, et al. Monsoon-induced partial carbonate platform drowning (Maldives, Indian Ocean). Geology. 2009;37: 867–870. doi: 10.1130/G25702A.1
22. Betzler C, Eberli GP, Kroon D, Wright JD, Swart PK, Nath BN, et al. The abrupt onset of the modern South Asian Monsoon winds. Sci Rep. 2016;6: 29838. doi: 10.1038/srep29838 27436574
23. Naik D., Saraswat R, Lea DW, Kurtarkar S., Mackensen A. Last glacial-interglacial productivity and associated changes in the eastern Arabian Sea. Palaeogeogr Palaeoclimatol Palaeoecol. 2017;483: 147–156. doi: 10.1016/j.palaeo.2016.07.014
24. Reolid J, Reolid M, Betzler C, Lindhorst S, Wiesner MG, Lahajnar N. Upper Pleistocene cold-water corals from the Inner Sea of the Maldives: taphonomy and environment. Facies. 2017;63. doi: 10.1007/s10347-016-0491-7
25. Kroon D, Steens T, Troelstra SR. Onset of monsoonal related upwelling in the western Arabian Sea as revealed by planktonic foraminifers. In: Prell W, Niitsuma N, editors. Proceedings of the Ocean Drilling Program, Scientific Results. College Station, Texas: Ocean Drilling program; 1991. pp. 257–263.
26. Krahmann G, Krüger K. Physical oceanography during SONNE cruise SO235. PANGAEA. 2018; doi: 10.1594/PANGAEA.887805
27. Quadfasel D. Physical oceanography during RV SONNE cruise SO127, 17 December 1997 to 7 January 1998 from Port Klang to Malé. PANGAEA. Institut für Meereskunde, Universität Hamburg; 2017; doi: 10.1594/PANGAEA.881513
28. Shankar D, Vinayachandran PN, Unnikrishnan AS. The monsoon currents in the north Indian Ocean. Prog Oceanogr. 2002;52: 63–120. doi: 10.1016/S0079-6611(02)00024-1
29. Hemleben C, Spindler M, Anderson RO. Modern Planktonic Foraminifera. New York: Springer-Verlag New York; 1989. doi: 10.1007/978-1-4612-3544-6
30. Betzler C, Eberli GP, Alvarez Zarikian CA, Bialik OM, Blättler CL, Guo JA, et al. Proceedings of the International Ocean Discovery Program, 359. Coll Station TX (International Ocean Discov Program). 2017; doi: 10.14379/iodp.proc.359.102.2017
31. Curry WB, Matthews RK. Paleo-oceanographic utility of oxygen isotopic measurements on planktic foraminifera: Indian Ocean core-top evidence. Palaeogeogr Palaeoclimatol Palaeoecol. 1981;33: 173–191.
32. Darling KF, Wade CM, Kroon D, Brown AJL. Planktic foraminiferal molecular evolution and their polyphyletic origins from benthic taxa. Mar Micropaleontol. 1997;30: 251–266.
33. Barker S, Greaves M, Elderfield H. A study of cleaning procedures used for foraminiferal Mg/Ca paleothermometry. Geochemistry, Geophys Geosystems. 2003;4: 8407. doi: 10.1029/2003GC000559
34. Martin PA, Lea DW. A simple evaluation of cleaning procedures on fossil benthic foraminiferal Mg/Ca. Geochemistry, Geophys Geosystems. 2002;3: 8401. doi: 10.1029/2001GC000280
35. Greaves M, Caillon N, Rebaubier H, Bartoli G, Bohaty S, Cacho I, et al. Interlaboratory comparison study of calibration standards for foraminiferal Mg/Ca thermometry. Geochemistry, Geophys Geosystems. 2008;9: Q08010. doi: 10.1029/2008GC001974
36. Spezzaferri S, Kucera M, Pearson PN, Wade BS, Rappo S, Poole CR, et al. Fossil and Genetic Evidence for the Polyphyletic Nature of the Planktonic Foraminifera “Globigerinoides”, and Description of the New Genus Trilobatus. PLoS One. 2015;10: e0128108. doi: 10.1371/journal.pone.0128108 26020968
37. Erez J, Luz B. Experimental paleotemperature equation for planktonic foraminifera. Geochim Cosmochim Acta. 1983;47: 1025–1031. doi: 10.1016/0016-7037(83)90232-6
38. Mulitza S, Donner B, Fischer G, Paul A, Pätzold J, Rühlemann C, et al. The South Atlantic Oxygen Isotope Record of Planktonic Foraminifera. In: Wefer G, Mulitza S, Ratmeyer V, editors. The South Atlantic in the Late Quaternary: Reconstruction of Material Budgets and Current Systems. Berlin: Springer; 2004. pp. 121–142.
39. Kim S-T, O’Neil JR. Equilibrium and nonequilibrium oxygen isotope effects in synthetic carbonates. Geochim Cosmochim Acta. 1997;61: 3461–3475. doi: 10.1016/S0016-7037(97)00169-5
40. Shackleton NJ. Attainment of isotopic equilibrium between ocean water and the benthonic foraminifera Genus Uvigerina: Isotopic changes in the ocean during the last glacial. Colloq Int du CNRS. 1974;219: 203–210.
41. Friedman I, O’Neil JR. Compilation of stable isotope fractionation factors of geochemical interest. Professional Paper. U.S. Government Printing Office; 1977. doi: 10.3133/pp440KK
42. Pearson PN. Oxygen Isotopes in Foraminifera: Overview and Historical Review. In: Ivany LC, Huber BT, editors. Reconstructing Earth’s Deep-time Climate. The Paleontological Society Papers; 2012. pp. 1–38.
43. Hut G. Consultants’ group meeting on stable isotope reference samples for geochemical and hydrological investigations, International Atomic Energy Agency (IAEA). International Atomic Energy Agency. 1987.
44. Epstein S, Buchsbacm J, Lowenstam HA, Ukey HC. Revised carbonate-water isotopic temperature scale. Bull Geol Soc Am. 1953;64: 1315–1326.
45. Duplessy JC, Bé AWH, Blanc PL. Oxygen and carbon isotopic composition and biogeographic distribution of planktonic foraminifera in the Indian Ocean. Palaeogeogr Palaeoclimatol Palaeoecol. 1981;33: 9–46. doi: 10.1016/0031-0182(81)90031-6
46. Srivastava R, Ramesh R, Prakash S, Anilkumar N, Sudhakar M. Oxygen isotope and salinity variations in the Indian sector of the Southern Ocean. Geophys Res Lett. John Wiley & Sons, Ltd; 2007;34: L24603. doi: 10.1029/2007GL031790
47. Dahl KA, Oppo DW. Sea surface temperature pattern reconstructions in the Arabian Sea. Paleoceanography. 2006;21: PA1014. doi: 10.1029/2005PA001162
48. Blättler CL, Higgins JA, Swart PK. Advected glacial seawater preserved in the subsurface of the Maldives carbonate edifice. Geochim Cosmochim Acta. 2019;257: 80–95. doi: doi.org/10.1016/j.gca.2019.04.030
49. Rostek F, Ruhlandt G, Bassinot FC, Muller PJ, Labeyrie LD, Lancelot Y, et al. Reconstructing sea surface temperature and salinity using δ18O and alkenone records. Nature. 1993;364: 319–321. doi: 10.1038/364319a0
50. Tiwari M, Nagoji SS, Kartik T, Drishya G, Parvathy RK, Rajan S. Oxygen isotope-salinity relationships of discrete oceanic regions from India to Antarctica vis-à-vis surface hydrological processes. J Mar Syst. Elsevier B.V.; 2013;113–114: 88–93. doi: doi.org/10.1016/j.jmarsys.2013.01.001
51. LeGrande AN, Schmidt GA. Global gridded data set of the oxygen isotopic composition in seawater. Geophys Res Lett. 2006;33: L12604. doi: 10.1029/2006GL026011
52. Elderfield H, Yu J, Anand P, Kiefer T, Nyland B. Calibrations for benthic foraminiferal Mg/Ca paleothermometry and the carbonate ion hypothesis. Earth Planet Sci Lett. 2006;250: 633–649. doi: 10.1016/j.epsl.2006.07.041
53. Yu J, Elderfield H. Mg/Ca in the benthic foraminifera Cibicidoides wuellerstorfi and Cibicidoides mundulus: Temperature versus carbonate ion saturation. Earth Planet Sci Lett. 2008;276: 129–139. doi: 10.1016/j.epsl.2008.09.015
54. Pearson PN, Wade BS. Taxonomy and stable isotope paleoecology of well-preserved planktonic foraminifera from the uppermost Oligocene of Trinidad. J Foraminifer Res. 2009;39: 191–217. doi: 10.2113/gsjfr.39.3.191
55. Singh A, Jani RA, Ramesh R. Spatiotemporal variations of the δ18O-salinity relation in the northern Indian Ocean. Deep Res. Elsevier; 2010;57: 1422–1431. doi: 10.1016/j.dsr.2010.08.002
56. Bouvier-Soumagnac Y, Duplessy J-C. Carbon and oxygen isotopic composition of planktonic foraminifera from laboratory culture, plankton tows and recent sediment; implications for the reconstruction of paleoclimatic conditions and of the global carbon cycle. J Foraminifer Res. 1985;15: 302–320. doi: 10.2113/gsjfr.15.4.302
57. Peeters FJC. The distribution and stable isotope composition of living planktic foraminifera in relation to seasonal changes in the Arabian Sea. Free University, Amsterdam, The Netherlands. 2000.
58. Lynch-Stieglitz J, Curry WB, Slowey N. A geostrophic transport estimate for the Florida Current from the oxygen isotope composition of benthic foraminifera. Paleoceanography. 1999;14: 360–373. doi: 10.1029/1999PA900001
59. Nürnberg D, Bijma J, Hemleben C. Assessing the reliability of magnesium in foraminiferal calcite as a proxy for water mass temperatures. Geochim Cosmochim Acta. 1996;60: 803–814. doi: 10.1016/0016-7037(95)00446-7
60. Lea DW, Mashiotta TA, Spero HJ. Controls on magnesium and strontium uptake in planktonic foraminifera determined by live culturing. Geochim Cosmochim Acta. 1999;63: 2369–2379. doi: 10.1016/S0016-7037(99)00197-0
61. Mashiotta TA, Lea DW, Spero HJ. Glacial–interglacial changes in Subantarctic sea surface temperature and δ18O-water using foraminiferal Mg. Earth Planet Sci Lett. Elsevier; 1999;170: 417–432. doi: 10.1016/S0012-821X(99)00116-8
62. Elderfield H, Ganssen G. Past temperature and δ18O of surface ocean waters inferred from foraminiferal Mg/Ca ratios. Nature. 2000;405: 442–445. doi: 10.1038/35013033 10839536
63. Nürnberg D, Müller A, Schneider RR. Paleo-sea surface temperature calculations in the equatorial east Atlantic from Mg/Ca ratios in planktic foraminifera: A comparison to sea surface temperature estimates from U37K, oxygen isotopes, and foraminiferal transfer function. Paleoceanography. John Wiley & Sons, Ltd; 2000;15: 124–134. doi: 10.1029/1999PA000370
64. Dekens PS, Lea DW, Pak DK, Spero HJ. Core top calibration of Mg/Ca in tropical foraminifera: Refining paleotemperature estimation. Geochemistry, Geophys Geosystems. 2002;3. doi: 10.1029/2001GC000200
65. Whitko AN, Hastings DW, Flower BP. Past sea surface temperatures in the tropical South China Sea based on a new foraminiferal Mg calibration. MARsci. 2002; MARSci.2002.01.020101.
66. McConnell MC, Thunell RC. Calibration of the planktonic foraminiferal Mg/Ca paleothermometer: Sediment trap results from the Guaymas Basin, Gulf of California. Paleoceanography. 2005;20: PA2016. doi: 10.1029/2004PA001077
67. Cléroux C, Cortijo E, Anand P, Labeyrie L, Bassinot F, Caillon N, et al. Mg/Ca and Sr/Ca ratios in planktonic foraminifera: Proxies for upper water column temperature reconstruction. Paleoceanography. 2008;23: PA3214. doi: 10.1029/2007PA001505
68. Sadekov A, Eggins SM, De Deckker P, Kroon D. Uncertainties in seawater thermometry deriving from intratest and intertest Mg/Ca variability in Globigerinoides ruber. Paleoceanography. 2008;23: PA1215. doi: 10.1029/2007PA001452
69. Regenberg M, Steph S, Nürnberg D, Tiedemann R, Garbe-Schönberg D. Calibrating Mg/Ca ratios of multiple planktonic foraminiferal species with δ18O-calcification temperatures: Paleothermometry for the upper water column. Earth Planet Sci Lett. Elsevier B.V.; 2009;278: 324–336. doi: 10.1016/j.epsl.2008.12.019
70. Hollstein M, Mohtadi M, Rosenthal Y, Moffa Sanchez P, Oppo D, Martínez Méndez G, et al. Stable Oxygen Isotopes and Mg/Ca in Planktic Foraminifera From Modern Surface Sediments of the Western Pacific Warm Pool: Implications for Thermocline Reconstructions. Paleoceanography. 2017;32: 1174–1194. doi: 10.1002/2017PA003122
71. Martin PA, Lea DW, Rosenthal Y, Shackleton NJ, Sarnthein M, Papenfuss T. Quaternary deep sea temperature histories derived from benthic foraminiferal Mg/Ca. Earth Planet Sci Lett. 2002;198: 193–209. doi: 10.1016/S0012-821X(02)00472-7
72. Healey SL, Thunell RC, Corliss BH. The Mg/Ca-temperature relationship of benthic foraminiferal calcite: New core-top calibrations in the < 4°C temperature range. Earth Planet Sci Lett. 2008;272: 523–530. doi: 10.1016/j.epsl.2008.05.023
73. Lear CH, Rosenthal Y, Slowey N. Benthic foraminiferal Mg/Ca paleothermometry: A revised core-top calibration. Geochim Cosmochim Acta. 2002;66: 3375–3387.
74. Raitzsch M, Kuhnert H, Groeneveld J, Bickert T. Benthic foraminifer Mg/Ca anomalies in South Atlantic core top sediments and their implications for paleothermometry. Geochemistry, Geophys Geosystems. John Wiley & Sons, Ltd; 2008;9: Q05010. doi: 10.1029/2007GC001788
75. Tisserand AA, Dokken TM, Waelbroeck C, Gherardi J-M, Scao V, Fontanier C, et al. Refining benthic foraminiferal Mg/Ca-temperature calibrations using core-tops from the western tropical Atlantic: Implication for paleotemperature estimation. Geochemistry, Geophys Geosystems. John Wiley & Sons, Ltd; 2013;14: 929–946. doi: 10.1002/ggge.20043
76. Lo Giudice Cappelli E, Regenberg M, Holbourn A, Kuhnt W, Garbe-schönberg D, Andersen N. Refining C. wuellerstorfi and H. elegans Mg/Ca temperature calibrations. Mar Micropaleontol. 2015;121: 70–84. doi: org/10.1016/j.marmicro.2015.10.001
77. Kubota Y, Kimoto K, Itaki T, Yokoyama Y, Miyairi Y, Matsuzaki H. Bottom water variability in the subtropical northwestern Pacific from 26 kyr BP to present based on Mg/Ca and stable carbon and oxygen isotopes of benthic foraminifera. Clim Past. 2015;11: 803–824. doi: 10.5194/cp-11-803-2015
78. Sadekov A, Eggins SM, De Deckker P, Ninnemann U, Kuhnt W, Bassinot F. Surface and subsurface seawater temperature reconstruction using Mg/Ca microanalysis of planktonic foraminifera Globigerinoides ruber, Globigerinoides sacculifer, and Pulleniatina obliquiloculata. Paleoceanography. 2009;24: PA3201. doi: 10.1029/2008PA001664
79. Darling KF, Wade CM. The genetic diversity of planktic foraminifera and the global distribution of ribosomal RNA genotypes. Mar Micropaleontol. 2008;67: 216–238. doi: 10.1016/j.marmicro.2008.01.009
80. Pearson PN, Wade BS, Huber BT. Taxonomy, biostratigraphy, and phylogeny of Oligocene Globigerinitidae (Dipsidripella, Globigerinita, and Tenuitella). Cushman Found Foraminifer Res Spec Publ. 2018;46: 429–458.
81. Bé AWH, Anderson OR, Faber WW, Caron DA, Be AWH. Sequence of morphological and cytoplasmic changes during gametogenesis in the planktonic foraminifer Globigerinoides sacculifer (Brady). Micropaleontology. 1983;29: 310. doi: 10.2307/1485737
82. Gang L, Qiang L, Guangyan N, Pingping S, Yanzhi F, Liangmin H, et al. Vertical Patterns of Early Summer Chlorophyll a Concentration in the Indian Ocean with Special Reference to the Variation of Deep Chlorophyll Maximum. J Mar Biol. 2012;2012. doi: 10.1155/2012/801248
83. Singh AD, Jung SJA, Darling K, Ganeshram R, Ivanochko T, Kroon D. Productivity collapses in the Arabian Sea during glacial cold phases. Paleoceanography. 2011;26: PA3210. doi: 10.1029/2009PA001923
84. Mulitza S, Wolff T, Pätzold J, Hale W, Wefer G. Temperature sensitivity of planktic foraminifera and its influence on the oxygen isotope record. Mar Micropaleontol. 1998;33: 223–240. doi: 10.1016/S0377-8398(97)00040-6
85. Wang L. Isotopic signals in two morphotypes of Globigerinoides ruber (white) from the South China Sea: implications for monsoon climate change during the last glacial cycle. Palaeogeogr Palaeoclimatol Palaeoecol. 2000;161: 381–394. doi: 10.1016/S0031-0182(00)00094-8
86. Kuroyanagi A, Tsuchiya M, Kawahata H, Kitazato H. The occurrence of two genotypes of the planktonic foraminifer Globigerinoides ruber (white) and paleo-environmental implications. Mar Micropaleontol. 2008;68: 236–243. doi: 10.1016/j.marmicro.2008.04.004
87. Numberger L, Hemleben C, Hoffmann R, Mackensen A, Schulz H, Wunderlich J-M, et al. Habitats, abundance patterns and isotopic signals of morphotypes of the planktonic foraminifer Globigerinoides ruber (d’Orbigny) in the eastern Mediterranean Sea since the Marine Isotopic Stage 12. Mar Micropaleontol. Elsevier B.V.; 2009;73: 90–104. doi: 10.1016/j.marmicro.2009.07.004
88. Steinke S, Chiu H-Y, Yu P-S, Shen C-C, Löwemark L, Mii H-S, et al. Mg/Ca ratios of two Globigerinoides ruber (white) morphotypes: Implications for reconstructing past tropical/subtropical surface water conditions. Geochemistry, Geophys Geosystems. 2005;6: Q11005. doi: 10.1029/2005GC000926
89. Aurahs R, Treis Y, Darling K, Kucera M. A revised taxonomic and phylogenetic concept for the planktonic foraminifer species Globigerinoides ruber based on molecular and morphometric evidence. Mar Micropaleontol. 2011;79: 1–14. doi: 10.1016/j.marmicro.2010.12.001
90. Bijma J, Hemleben C. Population dynamics of the planktic foraminifer Globigerinoides sacculifer (Brady) from the central Red Sea. Deep Sea Res Part I Oceanogr Res Pap. 1994;41: 485–510. doi: 10.1016/0967-0637(94)90092-2
91. Bé AWH, Bishop JKB, Sverdlove MS, Gardner WD. Standing stock, vertical distribution and flux of planktonic foraminifera in the Panama Basin. Mar Micropaleontol. 1985;9: 307–333. doi: 10.1016/0377-8398(85)90002-7
92. Bijma J, Hemleben C, Huber BT, Erlenkeuser H, Kroon D. Experimental determination of the ontogenetic stable isotope variability in two morphotypes of Globigerinella siphonifera (d’Orbigny). Mar Micropaleontol. 1998;35: 141–160. doi: 10.1016/S0377-8398(98)00017-6
93. Spero HJ, Parker SL. Photosynthesis in the symbiotic planktonic foraminifer Orbulina universa, and its potential contribution to oceanic primary productivity. J Foraminifer Res. 1985;15: 273–281. doi: 10.2113/gsjfr.15.4.273
94. Gastrich MD. Ultrastructure of a new intracellular symbiotic alga found within planktonic foraminifera. J Phycol. 1987;23: 623–632. doi: 10.1111/j.1529-8817.1987.tb04215.x
95. Kroon D, Ganssen G. Northern Indian Ocean upwelling cells and the stable isotope composition of living planktonic foraminifers. Deep Sea Res. 1989;36: 1219–1236. doi: 10.1016/0198-0149(89)90102-7
96. Aze T, Ezard THG, Purvis A, Coxall HK, Stewart DRM, Wade BS, et al. A phylogeny of Cenozoic macroperforate planktonic foraminifera from fossil data. Biol Rev. 2011;86: 900–927. doi: 10.1111/j.1469-185X.2011.00178.x 21492379
97. Ravelo AC, Fairbanks RG, Philander SGH. Reconstructing tropical Atlantic hydrography using planktontic foraminifera and an ocean model. Paleoceanography. 1990;5: 409–431. doi: 10.1029/PA005i003p00409
98. Bé AW., Tolderlund D. Distribution and ecology of living planktonic foraminifera in surface waters of the Atlantic and Indian Oceans. In: Funnel B., Riedel W., editors. The Micropaleontology of Oceans. London: Cambridge University Press; 1971. pp. 105–149.
99. Coxall HK, Spezzaferri S. Taxonomy, biostratigraphy and phylogeny of Oligocene Catapsydrax, Globorotaloides and Protentelloides. Cushman Found Foraminifer Res Spec Publ. 2018;46: 79–124.
100. Baumfalk YA, Troelstra SR, Ganssen G, Van Zanen MJL. Phenotypic variation of Globorotalia scitula (foraminiferida) as a response to Pleistocene climatic fluctuations. Mar Geol. Elsevier; 1987;75: 231–240. doi: 10.1016/0025-3227(87)90106-X
101. Ortiz JD, Mix AC, Rugh W, Watkins JM, Collier RW. Deep-dwelling planktonic foraminifera of the northeastern Pacific Ocean reveal environmental control of oxygen and carbon isotopic disequilibria. Geochim Cosmochim Acta. 1996;60: 4509–4523. doi: 10.1016/S0016-7037(96)00256-6
102. Spezzaferri S. Planktonic foraminiferal paleoclimatic implications across the Oligocene-Miocene transition in the oceanic record (Atlantic, Indian and South Pacific). Palaeogeogr Palaeoclimatol Palaeoecol. 1995;114: 43–74.
103. Rippert N, Max L, Mackensen A, Cacho I, Povea P, Tiedemann R. Alternating Influence of Northern Versus Southern-Sourced Water Masses on the Equatorial Pacific Subthermocline During the Past 240 ka. Paleoceanography. 2017;32: 1256–1274. doi: 10.1002/2017PA003133
104. Schiebel R, Hemleben C. Interannual variability of planktic foraminiferal populations and test flux in the eastern North Atlantic Ocean (JGOFS). Deep Sea Res. 2000;47: 1809–1852. doi: 10.1016/S0967-0645(00)00008-4