[6] Here we investigate the use of Li/Ca ratios, and the combination with Mg/Ca as Mg/Li and Li/Mg ratios, as sea surface temperature proxies in tropical corals. We utilize modern Porites corals from locations with exceptional local in situ temperature data to calibrate these promising new proxies while revealing some potential caveats to their use that highlight the complexity of biomineralization processes.

[5] Inorganic precipitation experiments suggest that Li + is incorporated into aragonite by heterovalent substitution of Ca 2+ in the CaCO 3 structure [ Okumura and Kitano , 1986 ; Marriott et al ., 2004b ]. Although there are many studies of Mg incorporation into CaCO 3 [e.g., M orse and Bender , 1990 ; Rimstidt et al ., 1998 , and references therein], the mode of incorporation into coral aragonite is not established [e.g., Allison et al ., 2011 ; Gaetani et al ., 2011 ]. The results of X‐ray Absorption Near Edge Structure (XANES) studies are difficult to interpret but suggest Mg exists in Porites coral samples as magnesite (MgCO 3 ) [ Farges et al ., 2009 ]. In contrast, another XANES study of corals suggests Mg is present as a disordered phase or is associated with organics [ Finch and Allison , 2008 ]. Culturing of Porites corals shows little direct temperature control on Mg/Ca ratios but indicates Mg/Ca increases with the extension rate of the coral [ Inoue et al ., 2007 ]. However, the lack of a measureable Li isotope fractionation within corals skeletons argues against a kinetic control on Li incorporation into coral aragonite [ Marriott et al ., 2004a ; Rollion‐Bard et al ., 2009 ]. Although the existing data concerning the controls of Li and Mg incorporation into biogenic aragonite are often difficult to reconcile, the similarities (apparent partition coefficients <<1) and differences (heterovalent 2Li + versus homovalent Mg 2+ incorporation) between these two elements means their combined study can potentially improve the understanding of trace metal incorporation into biogenic aragonite.

[4] Studies of the Li/Ca ratio of calcite foraminifera shells have generally not reproduced the clear temperature dependence displayed by inorganic calcite but instead suggest Li/Ca is influenced by growth rate and therefore seawater carbonate ion concentration [ Delaney et al ., 1985 ; Hall and Chan , 2004 ; Hathorne and James , 2006 ; Lear and Rosenthal , 2006 ]. More recently, the combination of Li/Ca with the known temperature proxy of foraminiferal Mg/Ca, as Mg/Li ratios has been shown to correlate better with deep sea temperatures than Mg/Ca ratios alone [ Bryan and Marchitto , 2008 ]. Interestingly, the largest improvement found by using Mg/Li instead of Mg/Ca ratios in benthic foraminifera was for the aragonitic species H . elegans [ Bryan and Marchitto , 2008 ]. This work inspired others to investigate Li/Ca and Mg/Li ratios, and clear relationships with deep sea temperature have been observed in various species of aragonitic cold water corals [ Case et al ., 2010 ; J. Raddatz et al., Temperature dependence of stable Sr isotopes, Sr/Ca and Mg/Li in the scleractinian cold water coral Lophelia pertusa , submitted to Chemical Geology . 2012; hereinafter referred to as Raddatz et al., submitted manuscript, 2012].

[3] Calcium carbonate has two major polymorphs in nature, trigonal calcite with six‐fold coordination and orthorhombic aragonite with ninefold coordination. Although tropical corals build their skeletons from aragonite, it is nonetheless informative to consider trace element incorporation into calcite and aragonite. The lithium content of inorganic calcite was observed to be negatively correlated with temperature in laboratory precipitation experiments conducted with low‐salinity solutions [ Marriott et al ., 2004a ]. The same study also analyzed lithium in the aragonite skeleton of a Porites coral from Jarvis Island at a sampling resolution of approximately four samples per year. Over two to three seasonal SST and coral δ 18 O cycles, the Li/Ca values suggested an inverse relationship with temperature where coral Li/Ca decreased by 5% for every degree of temperature increase [ Marriott et al ., 2004a ]. This temperature dependence is large compared to that of only around 0.7% per degree for Sr/Ca [e.g., Corrège , 2006 ]. This makes coral Li/Ca a very promising tool for SST reconstructions, even when considering the lower concentration of Li in coral aragonite (µmol/mol versus mmol/mol) and the poorer measurement precision likely to be obtained as a result. A further study found no influence of salinity on the Li/Ca ratio of inorganically precipitated aragonite [ Marriott et al ., 2004b ]. This is more evidence that the Li/Ca ratio of aragonite could be a robust proxy for SST, but unfortunately these authors did not perform inorganic aragonite precipitation experiments at different temperatures.

[2] The possibility to extend the instrumental record of sea surface temperatures (SSTs) by analyzing the chemistry of the aragonite skeletons of tropical corals has been explored and utilized in recent decades [ Beck et al ., 1992 ; Shen et al ., 1992 ; McCulloch et al ., 1994 ; Tudhope et al ., 2001 ; Quinn and Sampson , 2002 ; Corrège et al ., 2004 ; Felis et al ., 2004 ; Kilbourne et al ., 2004 ; Ayling et al ., 2006 ]. The proxies that have been developed and widely applied for SST are δ 18 O [e.g., Tudhope et al ., 2001 ], Sr/Ca [e.g., Gagan et al ., 1998 ], and U/Ca [e.g., Min et al ., 1995 ]. The δ 18 O composition of corals is also a function of the δ 18 O of seawater (which is correlated with salinity regionally) and therefore compliments a true SST proxy by enabling paleo‐δ 18 Owater (salinity) estimates [e.g., Ren et al ., 2003 ]. Although U/Ca has been observed to correlate well with SST in various locations [e.g., Min et al ., 1995 ; Felis et al ., 2009 , 2010 ] the pH dependence of U speciation in seawater [e.g., Raitzsch et al ., 2011 ] suggests coral U/Ca should also be affected by seawater carbonate chemistry (salinity), as recently confirmed by culturing experiments [ Inoue et al ., 2011 ]. Coral Sr/Ca has been shown to be a robust SST proxy under various conditions [e.g., Gagan et al ., 1998 ], but concerns have been raised about variability in surface water Sr/Ca ratios [e.g., Brass and Turekian , 1974 ; de Villiers , 1999 ] and the possibility of changes in global seawater Sr/Ca ratios over glacial–interglacial cycles [ Stoll and Schrag , 1998 ]. Therefore, the development of other proxies for SST in tropical corals is desirable.

[9] The proxy calibration followed established methods [ Felis et al ., 2004 , 2009 ]. The annual Li/Ca maxima and minima for the OGA coral were tied to the corresponding extreme values in a local monthly SST record (1975–1994; Tokyo Metropolitan Ogasawara Fisheries Center) and subsequently interpolated to bimonthly intervals using the AnalySeries software (freely available at http://www.lsce.ipsl.fr/logiciels/index.php ). The annual Li/Ca maxima and minima for the Tahiti coral were tied to the corresponding extreme values in a local monthly SST record (1987–1991) [ Gerard , 1992 ] and subsequently interpolated to monthly intervals in the same manner. A linear least squares regression was then carried out for interpolated Li/Ca, Mg/Ca, Mg/Li, Li/Mg, and SST data with SST as the independent variable. The Li/Ca‐based age model occasionally (7 out of 43 tie points) differs by one or two samples from the Sr/Ca‐ and U/Ca‐based age models used in previous calibrations of the OGA coral [ Felis et al ., 2009 ]. Similarly, the Li/Ca‐based age model for the Tahiti coral differs little from the Sr/Ca‐based age model used in a previous calibration [ Felis et al ., 2012 ].

[8] For ICP‐MS analysis, ~300 µg of coral powder was weighed and placed into a small (8–30 mL) acid‐cleaned HDPE bottle. The powder was dissolved by adding 5–25 mL of 0.3M HNO 3 made from thermally distilled HNO 3 diluted with 18.2 MΩ cm H 2 O (Milli‐Q). After equilibration for at least 12 h, 100–1000 μL of sample solution was removed and diluted with 0.3M HNO 3 to have a Ca concentration of 10 ppm in an acid‐cleaned PE centrifuge tube. Analyses were performed using either an Element 2 (Thermo Scientific) sector field ICP‐MS at the University of Bremen or the Agilent 7500cs ICP‐MS at the GEOMAR, Kiel. The majority of the data were measured in Bremen, with only the additional sampling transect of the OGA coral measured in Kiel. The isotopes monitored during this study were 7 Li, 24 Mg, 25 Mg, 27 Al, 43 Ca, 48 Ca, 55 Mn, 88 Sr, 137 Ba, and 238 U. Raw intensities were blank corrected and normalized to 43 Ca before element/Ca ratios were calculated using the technique of Rosenthal et al . [ 1999 ]. A standard solution was prepared from single‐element solutions to have known element/Ca ratios similar to the samples and a Ca concentration of 10 ppm. All samples with Ca intensities >15% larger or smaller than the standard were rediluted accordingly and run again. Aliquots of the JCp‐1 Porites coral powder reference material [ Okai et al ., 2002 ] were analyzed as unknowns to ensure consistency between measurement sessions and the two laboratories. The average JCp‐1 value and standard deviation ( n = 25) during the course of this study was 6.29 ± 0.13 µmol/mol for Li/Ca, 4.17 ± 0.05 mmol/mol for Mg/Ca, 1.51 ± 0.04 mmol/mol for Li/Mg, 0.66 ± 0.02 mol/mmol for Mg/Li, and 1.18 ± 0.01 µmol/mol for U/Ca. Based on these analyses the external precision at the 95% confidence level (2σ) is estimated to be 4% for Li/Ca, 2.7% for Mg/Ca, 5.1% for Li/Mg and Mg/Li, and 2% for U/Ca.

[7] The details of the Porites coral (OGA‐02‐1) from the Ogasawara Islands (Japan) located at ~27° N in the western subtropical North Pacific (hereafter OGA coral) are given in Felis et al . [ 2009 ]. Local SST was measured during the calibration period ~1200 m from the OGA coral site (Tokyo Metropolitan Ogasawara Fisheries Center). A Porites coral (TAH‐95) was drilled at a water depth of 4–5 m on the north side of Tahiti (French Polynesia) located at ~17.5° S in the central tropical South Pacific (hereafter Tahiti coral) [ Felis et al ., 2012 ]. Local SST was measured during the calibration period ~850 m from the Tahiti coral site [ Gerard , 1992 ]. Coral samples were slabbed, X‐rayed, and microsampled following established methods [ Felis et al ., 2000 , 2004 ], with an average temporal resolution of >7 samples/yr for the OGA coral and of >17 samples/yr for the Tahiti coral. Aliquots of this powder were analyzed for stable isotopes as well as Sr/Ca and U/Ca ratios [ Felis et al ., 2009 , 2012 ], and the same powder was used for the ICP‐MS analyses reported here. Growth rates for the OGA coral during the studied period were 1.0–1.7 cm/yr with an average of 1.3 cm/yr [ Felis et al ., 2009 ] and were about 1.2–1.6 cm/yr with an average of 1.4 cm/yr for the Tahiti coral [ Felis et al ., 2012 ].

[11] The Li/Ca ratio of the Tahiti coral displays clear annual cycles ranging from 5.88 to 7.22 µmol/mol that track the local SST well (Figure 3 ). The Mg/Ca ratios of the Tahiti coral sometimes show clear annual cycles and range from 4.71 to 5.18 mmol/mol. The Li/Mg and Mg/Li ratios for the Tahiti coral also display clear annual cycles like the Li/Ca ratios and range from 1.47 to 1.18 and 0.68 to 0.85 mol/mmol, respectively.

[10] The original element/Ca data for the OGA and Tahiti corals are presented in Table S1 (auxiliary materials are available at http://www.pangaea.de ). The Li/Ca ratio of the OGA coral varies from 6.01 to 9.07 µmol/mol and displays clear annual cycles that match the SST records well (Figure 1 ). The amplitude of the Li/Ca cycles follows the interannual variability of local SST better than that of a gridded SST product that represents a 1° × 1° area (HadISST1.1; see Rayner et al . [ 2003 ]). During the period between 1979 and 1980 the Li/Ca ratio does not track the SST well, and there are two anomalously high Li/Ca values that will be discussed in detail in section 4.2 . Mg/Ca ratios of the OGA coral sometimes show clear annual cycles and range from 3.63 to 4.88 mmol/mol, with the exception of the period between 1979 and 1980, where the Mg/Ca ratios are 5 mmol/mol or greater, peaking at over 8 mmol/mol. The Li/Mg and Mg/Li ratios for the OGA coral display clear annual cycles like the Li/Ca ratios and range from 2.07 to 1.32 and 0.5 to 0.7 mol/mmol, respectively. The exception is the period between 1979 and 1980, where values are anomalously low or high (only Li/Mg shown in Figure 1 ). The measurements of the period between 1979 and 1980 were repeated, and an additional transect through the same density bands of the coral was also sampled and analyzed. These data confirm the presence of anomalously high Li/Ca and Mg/Ca values (Figure 2 ), while the Mn/Ca and Al/Ca ratios, which are considered indicators of contamination from Mn oxides and clays, are below suspect levels (Table S1).

4 Discussion

4.1 Calibration of Li/Ca, Mg/Li and Li/Mg Ratios With Local SST [12] Regression analysis of the OGA coral Li/Ca excluding the data from samples with Mg/Ca ratios >5 mmol/mol reveals a strong relationship (r2 = 0.73, p < 0.0001) between Li/Ca and SST. A linear least squares regression was also carried out for bimonthly interpolated Mg/Ca, Mg/Li, and Li/Mg ratios with local SST, and the monthly interpolated data for the Tahiti coral were analyzed in the same way (Figure 4). The resulting relationships are detailed in Table 1. The Mg/Ca ratio of the OGA coral was very weakly correlated with SST, while no significant relationship could be found for the Tahiti coral (Table 1). The slopes for the Tahiti coral Li/Ca‐SST and Mg/Li‐SST relationships are twice as steep as those found for the OGA coral. A similar range of temperature sensitivities is also observed for other coral‐based proxies [Corrège, 2006; Gagan et al., 2012, and references therein]. It is interesting to note that the Tahiti Li/Ca data fall directly on those for the OGA coral (Figure 4). Therefore, if only the data from above 26°C were regressed, a similar result would be obtained for both corals. This suggests there may be some degree of nonlinearity to the Li/Ca‐SST relationship, but calibrations using small temperature ranges may not be representative. The OGA coral Li/Ca‐SST relationship decreases by 1.8% per °C (at 25°C), while the Tahiti coral Li/Ca‐SST relationship decreases by 3.9% and is more similar to the 5% per °C reported for a Jarvis Island Porites coral [Marriott et al., 2004a]. Although it is difficult to assign temperatures accurately without the original SST data, the SST estimates derived by applying the Tahiti coral Li/Ca‐SST relationship to the Li/Ca ratios from the Jarvis Island coral fit the SST shown in Marriott et al. [2004a] well. This suggests the higher slope of the Li/Ca data from temperatures above 26°C may be widely applicable to Porites corals across the tropics. Figure 4 Open in figure viewer PowerPoint Regression analysis of the Li/Ca, Mg/Ca, Mg/Li, and Li/Mg ratios of OGA and Tahiti corals with locally measured SST. See Table 1 for more details. Table 1. Results for Ordinary Least Squares Regression of Coral Element/Ca Ratios With Local SST Intercept b Slope a Regression Coefficient r2 OGA Li/Ca 9.97 (±0.18) ‐0.123 (±0.007) 0.73 OGA Mg/Ca 3.16 (±0.20) 0.050 (±0.008) 0.26 OGA Mg/Li 0.19 (±0.029) 0.018 (±0.0012) 0.69 OGA Li/Mg 2.76 (±0.08) ‐0.048 (±0.003) 0.67 Average annual OGA Li/Ca 14.4 (±2.2) ‐0.31 (±0.09) 0.45 Average annual OGA Mg/Li ‐0.40 (±0.4) 0.042 (±0.016) 0.32 Average annual OGA Li/Ca 4.30 (±1.0) ‐0.11 (±0.04) 0.32 Tahiti Li/Ca 14.0 (±0.7) ‐0.277 (±0.025) 0.68 Tahiti Mg/Li ‐0.19 (±0.09) 0.035 (±0.003) 0.65 Tahiti Li/Mg 2.96 (±0.16) ‐0.060 (±0.006) 0.64 [13] To test that the relationship between Li/Ca and SST is not an artifact of the annual cycle of another variable causing the Li/Ca ratio to fluctuate, we have conducted a regression of the average annual Li/Ca ratios of the OGA coral with local SST [Crowley et al., 1999; Evans et al., 1999; Felis et al., 2009]. Although the seasonal temperature range at the OGA location is large, the average annual temperatures vary by only ~1°C, making the regression with Li/Ca ratios relatively imprecise (Table 1). Even so, the regression of the annual average OGA Li/Ca with SST gives r2 = 0.45 (p < 0.005). There is no significant relationship between the annual average OGA Li/Ca ratio and the average annual sea surface salinity [Carton and Giese, 2008], suggesting the variance of Li/Ca ratios is dominated by SST and is relatively insensitive to seawater chemistry. Furthermore, the slope and intercept of the OGA coral average annual Li/Ca‐SST relationship are very similar to the seasonal relationship from the Tahiti coral and the OGA coral for temperatures above 26°C. This strongly suggests that the differences between seasonal and average annual Li/Ca‐SST calibrations, also documented for Sr/Ca, U/Ca, and δ18O ratios of the OGA coral (see supplementary information of Felis et al. [2009]), result from the nonlinearity of the relationship between Li/Ca and SST. Recently it was suggested that two types of calibration are required for coral SST reconstructions using Sr/Ca and δ18O ratios, one for seasonal and one for multiannual reconstructions [Gagan et al., 2012]. These authors suggest the differences in proxy sensitivity result from variable “bio‐smoothing” attenuating the proxy signal for different coral colonies. However, it seems that variability in the sensitivity of coral Li/Ca potentially occurs within a single colony at different times of the year. The fact that the data from higher temperatures agree points to a lower sensitivity of Li/Ca at lower temperatures. In some Porites corals from other Japanese islands, a reduction of extension rate and the formation of a high‐density band has been observed during the winter months [Mitsuguchi et al., 2003]. This is not the case for the OGA coral, as the high‐density band is precipitated during summer, and the other geochemical records do not indicate reduced growth during winter [Felis et al., 2009]. [14] Interestingly, the slopes and intercepts of the Li/Mg‐SST relationships are similar for both OGA and Tahiti corals (Table 1). As the Ca concentration in the coral aragonite varies by <1% [e.g., Gaetani and Cohen, 2006], there should be no induced correlations from comparing Li/Ca with Mg/Ca ratios [Lenahan et al., 2011]. Thus it appears that using Mg/Ca as the denominating ratio accounts for some of the nonlinearity of the Li/Ca‐SST relationship above 26°C. More corals from diverse locations should be measured, but it may be that Li/Mg ratios help to overcome some intercoral offsets in paleothermometry. [15] Using the maximum and minimum slopes from the standard error (Table 1) to calculate the range of element ratios and the resulting range of estimated SST produces uncertainties of between ±1.0 and 1.7°C for Li/Ca and ±1.1 and 1.9°C for Li/Mg. This is comparable to Sr/Ca slope uncertainties [e.g., Felis et al., 2004, 2009], making Li/Ca and Li/Mg ratios useful additions to the coral paleothermometer arsenal.

4.2 Anomalously High Li/Ca and Mg/Ca Ratios [16] The anomalously high Li and Mg in the 1979–1980 section of the OGA coral are not the result of contamination by Mn oxides or clays, as confirmed by the analysis of an additional transect through the same density bands. Manganese was below detection in all samples, and Al/Ca ratios were <100 µmol/mol and were often below detectable levels (Table S1). The zone of high Li and Mg is slightly wider in the additional transect than the primary transect, probably the result of a slightly higher growth rate in the additional transect. The X‐ray of the coral looks normal throughout the 1979 and 1980 section, and the Sr/Ca, U/Ca and δ18O ratios measured in this section are within normal ranges and follow the SST well [Felis et al., 2009]. This is also the case for the U/Ca (Figure 2) and Sr/Ca ratios (not shown) measured in the additional transect. The δ13C through this section of coral [Felis et al., 2009] does not suggest the anomalous Li and Mg could have resulted from biological effects related to symbiont photosynthesis and coral metabolism [e.g., Gagan et al., 1994; Felis et al., 1998; Grottoli, 2002]. Secondary aragonite crystals are known to form in modern corals [e.g., Hendy et al., 2007; Sayani et al., 2011], but these have lower Mg/Ca ratios than primary skeleton [e.g., Hathorne et al., 2011]. A thin section from the 1979–1980 section of the OGA coral shows no indication of diagenesis. All this points to the anomalously high Li and Mg occurring in the original coral skeleton. It is interesting to note that the Li/Ca and Mg/Ca ratios are positively correlated with each other in the section where they are anomalously high (Figure 2). This contrasts with the areas of skeleton where Li/Ca ratios closely follow SST and the Li/Ca and Mg/Ca ratios are generally negatively correlated (Figures 1 and 3). High Li and Mg contents have been found associated with centers of calcification (COC) in some cold water corals [Case et al., 2010]. Therefore, the anomalously high Li/Ca and Mg/Ca ratios could potentially have resulted from a higher proportion of COC in this section of the skeleton. Inspection of the current thin sections provides no clear evidence, and different section preparation techniques to highlight COC and image analysis techniques will need to be developed to quantify COC proportion. Even if the underlying mechanism remains elusive, all evidence suggests the anomalously high Li/Ca and Mg/Ca ratios result from a biological effect on the incorporation into the biogenic aragonite.

4.3 Incorporation of Li and Mg Into Biogenic Aragonite [17] The Li/Mg SST relationship obtained for the OGA coral is similar to those found by previous studies of cold water corals [Case et al., 2010; Raddatz et al., submitted manuscript, 2012] and aragonitic benthic foraminifera H. elegans [Bryan and Marchitto, 2008] (Figure 5). The Li/Ca SST relationship is slightly stronger than that for Mg/Li (and Li/Mg), in contrast to previous studies where a stronger relationship was found between Mg/Li ratios and water temperature [Bryan and Marchitto, 2008; Case et al., 2010]. More data from diverse calcifiers are needed, but the comparison of the available Li/Mg (or Mg/Li) data from biogenic aragonite can be explained with a single exponential relationship to water temperature (Figure 6). This hints at the possibility of an overarching mechanism controlling the temperature response of Li and Mg incorporation into aragonite. Figure 5 Open in figure viewer PowerPoint Relationships between Li/Mg ratios with water temperature obtained by this study and from the literature. Figure 6 Open in figure viewer PowerPoint Exponential relationship between Li/Mg ratios and water temperature obtained by this study and others plotted on a log scale. Symbols are the same as in Figure 5 [18] As noted in section 1, the incorporation of Li and Mg into biogenic CaCO 3 is poorly understood. Even so, it is important to consider the possible mechanisms for the temperature influence on coral Li/Ca ratios and the anomalously high Li/Ca and Mg/Ca ratios in the 1979–1980 section of the OGA coral. A positive correlation between Mg/Ca ratios and SST has been reported for some Porites corals [e.g., Mitsuguchi et al., 1996; Sinclair et al., 1998], but the relationship is often not clear or consistent [e.g., Mitsuguchi et al., 2008]. This is also evident in the poor and insignificant correlation of Mg/Ca with local SST in this study (section 4.1), although some years have clear annual cycles of Mg/Ca. It must be noted that no oxidative cleaning of the coral powder was performed in this study, as is sometimes undertaken before Mg/Ca analysis [e.g., Mitsuguchi et al., 1996, 2003]. [19] Rayleigh fractionation from a closed reservoir combined with a temperature‐dependent reservoir depletion has been used to explain the positive relationship between coral Mg/Ca and temperature, as the Mg/Ca ratio of the reservoir would increase as Ca is progressively depleted [Gaetani and Cohen, 2006; Cohen and Gaetani, 2010]. Case et al. [2010] attributed the strong positive correlation between Li/Ca and Mg/Ca ratios within the skeletons of cold water corals to the fact that the apparent partition coefficients of both Li and Mg are <<1, and they would respond to Rayleigh fractionation similarly. However, within the skeletons of the tropical Porites corals examined here the Li/Ca and Mg/Ca ratios are anticorrelated apart from the period of anomalously high Li/Ca and Mg/Ca (Figures 1-3). This difference may simply result from the difference in the sampling scales between the <100 µm laser ablation sampling of Case et al. [2010] and the <1000 µm drill sampling of this study. Additionally, the large Li/Ca and Mg/Ca variability seen in deep‐sea corals, which experience only small changes in temperature, reveals the extent of reservoir depletion and Rayleigh fractionation is not temperature dependent. We suggest that the positively correlated ratios during the period of anomalously high Li/Ca and Mg/Ca of a Porites coral resulted from biological effects unrelated to temperature, possibly Rayleigh fractionation during biomineralization. However, under normal circumstances where such effects are minimal, Li/Ca and Mg/Ca ratios are negatively or poorly correlated, and the Li/Ca ratio faithfully reflects SST. [20] Given the clear nonenvironmental controls on tropical coral Mg/Ca ratios observed here and elsewhere [e.g., Meibom et al., 2008], the underpinning use of Mg/Ca ratios in multielement coral thermometry [Cohen and Gaetani, 2010; Gaetani et al., 2011] should be reconsidered. Li/Ca ratios should be very helpful for such multielement techniques, as the apparent partition coefficient of Li is <<1.