Past ocean acidification recorded in the geological record facilitates the understanding of rates and influences of contemporary pCO2 enrichment. Most pH reconstructions are made using boron, however there is some uncertainty associated with vital effects and isotopic fractionation. Here we present a new structural proxy for carbonate chemistry; Mg-O bond strength in coralline algae. Coralline algae were incubated in control (380 μatm pCO2), moderate (750 μatm pCO2), and high (1000 μatm pCO2) acidification conditions for 24 months. Raman spectroscopy was used to determine skeletal Mg-O bond strength. There was a positive linear relationship between pCO2 concentration and bond strength mediated by positional disorder in the calcite lattice when accounting for seasonal temperature. The structural preservation of the carbonate chemistry system in coralline algal high-Mg calcite represents an alternative approach to reconstructing marine carbonate chemistry. Significantly, it also provides an important mechanism for reconstructing historic atmospheric CO2 concentrations.
Atmospheric CO2 concentrations have increased from 275 µatm in A.D. 1700 (Keeling and Whorf, 1999) to 400 µatm today (Tans, 2014) with the oceans absorbing 25%–30% of the CO2 released into the atmosphere (Bates et al., 2012). The dissolved CO2 reacts with water to form carbonic acid, and as CO2 levels increase at the atmosphere-ocean interface, the carbonic acid is reduced to H+ and . This secondary process reduces carbonate saturation states and pH, a process called ocean acidification (OA) (Doney et al., 2009).
Such changes in carbonate saturation states can impact the marine biosphere. As the carbonate system changes, increased enables calcification to continue; however, calcifiers will be prone to dissolution and metabolic disruptions (Roleda et al., 2012). Although many marine organisms are expected to be adversely affected by OA (Hall-Spencer et al., 2008b; Kuffner et al., 2007; Ries et al., 2009), interspecies variability in susceptibility exists (Fabricius et al., 2011; Inoue et al., 2013). Poorly understood organismal tradeoffs to survive OA mean new approaches are now required to understand sensitivities (Dupont and Portner, 2013; Hall-Spencer et al., 2008a).
During the Paleocene-Eocene Thermal Maximum (PETM) large quantities of carbon dissolved into the oceans causing OA, and while current anthropogenically driven CO2 release is projected to be of similar magnitude, it will be at a higher rate than during the PETM (Zachos et al., 2005). Thus such paleoclimate events can also be used to assess rates and influences of acidification change in recent centuries.
High-resolution reconstructions of oceanic pH or pCO2 are used to understand changes in the carbon cycle, including OA (Honisch et al., 2012). Boron has been used to reconstruct seawater pH patterns from marine carbonates, with the role of δ11B as a pH proxy validated with interlaboratory calibrations (Foster et al., 2013). For example, boron isotopes have been used to reconstruct OA during the PETM (Penman et al., 2014), the Miocene Climatic Optimum (Foster et al., 2012), and the last deglaciation (Henehan et al., 2013). Uncertainty associated with proxy-derived vital effects and isotopic fractionation requires further refining to reduce propagation errors (Babila et al., 2014).
Red coralline algae are high-resolution paleoenvironmental proxies with wide geographical distribution (Henrich et al., 1995), long lifespan (Foster, 2001), seasonal growth banding (Adey and McKibbin, 1970; Foster, 2001), and, in several species, reduced structural and physiological susceptibility to changes in carbonate chemistry (Burdett, 2014; Kamenos et al., 2013; Martin et al., 2013; McCoy and Ragazzola, 2014; Nash et al., 2013). In Lithothamnion glaciale, a high-latitude species, there is a response of Mg-O bond strength to marine carbonate chemistry within the algal skeleton driven by the rate of pH reduction (Kamenos et al., 2013). The dependency of crystal lattice integrity on carbonate chemistry variability indicates the potential for Mg-O bond strength to act as a carbonate chemistry proxy.
In this study, we investigate the application of coralline algal skeletal Mg-O bond strength as a carbonate chemistry proxy. It is expected that (1) individuals will show seasonal patterns in Mg composition, (2) moderate and high OA treatments (high pCO2, low pH) will alter coralline algal structural integrity, altering their Mg-O bond strength, and (3) a relationship exists between Mg-O bond strength and carbonate chemistry.
Lithothamnion glaciale (Fig. 1) from Scotland (Fig. 2) were cultured for 2 yr at 380, 750, and 1000 µatm pCO2 following ambient temperature and light. Full carbonate chemistry of each treatment was calculated. Mg concentrations and Mg-O bond strength of the high-Mg calcite skeleton deposited prior to and during the experiment (n = 5 thalli per treatment) were determined using Raman spectroscopy (spot size = 15 µm). Relative Mg concentrations were determined from the position of the ∼1089 cm–1 Raman shift peak. Mg-O bond strength was determined from the full width at half peak maximum (FWHM) of the ∼1089 cm–1 peak (Bischoff et al., 1985; Kamenos et al., 2013). In L. glaciale, Mg is a component of the crystal lattice (Kamenos et al., 2009), and thus increases in Mg-O bond strength can be attributed to increasing positional disorder of crystal lattice bringing Mg and O closer together via Mg ions moving out of the plane parallel to the a-axis in the direction of the c-axis (Fig. DR1 in the GSA Data Repository1) (Bischoff et al., 1985). Thus reduced FWHM is caused by increased positional disorder, which in turn caused stronger Mg-O bonds. For full methods, see the Data Repository.
Lithothamnion glaciale exhibited seasonal variation in skeletal parameters. Relative Mg concentrations were higher in summer while Mg-O bond strengths were weaker. Both parameters gradually declined and increased respectively across the seasonal transition into winter (Fig. 3).
Influence of pCO2 on Structural Properties
While relative Mg concentrations were lower in all treatments after laboratory incubation (Fig. 3), a significant difference occurred only in the 1000 µatm pCO2 treatment (F = 21.96, df = 1 [degrees of freedom], p < 0.001). The control treatment exhibited a significant relationship between relative Mg concentrations and seasonal stage (Fig. 3) (F = 3.39, df = 1, p = 0.02). This relationship was present, but non-significant, in the pCO2 enrichment treatments (750 µatm: F = 1.29, df = 5, p = 0.304; 1000 µatm: F = 1.03, df = 5, p = 0.425). Bond strengths were higher in all treatments following incubation (Fig. 3), but with significant differences occurring only in the pCO2 enrichment treatments (380 µatm: F = 0.68, df = 1, p = 0.420; 750 µatm: F = 9.65, df = 1, p < 0.01; 1000 µatm: F = 18.65, df = 1, p < 0.01).
Mg-O bond strength within the high-Mg calcite skeleton of the coralline alga L. glaciale increases with increasing marine pCO2 concentrations; this forms the basis for its utility as a pCO2 proxy. While pCO2 and other carbonate chemistry parameters can co-vary, pCO2 was used to control the experimental carbonate chemistry and was the most stable carbonate parameter, so it was deemed to be the forcing factor driving changes in Mg-O bond strength. pCO2 acts on coralline algae via in the carbonate chemistry system; is used as the substrate for calcification and as a carbon supplier during photosynthesis (Digby, 1977; Johnson et al., 2014; Koch et al., 2013).
Natural Seasonal Variability
Coralline algae show natural seasonal variability in Mg-O bond strength, with lower strengths present during summer months across treatments (Fig. 3). Structurally, bond strength increases as a consequence of increased position disorder when Mg ions move out of the a-axis into the c-axis (Bischoff et al., 1985). Thus during summer, the skeleton exhibits the least positional disorder in the calcite lattice. This may be due to optimal summer light and temperature conditions required for photosynthesis (Ries et al., 2009), causing better-controlled skeletal deposition.
The seasonal change in Mg concentrations (Figs. 3 and 4) is due to a positive correlation between Mg concentration and in situ temperatures driven by the abiotic replacement of Ca2+ by Mg2+ ions within the calcite lattice at higher temperatures (Kamenos et al., 2009). For L. glaciale, this relationship has been confirmed using electron microprobe analysis at this collection location (Kamenos, 2010; Kamenos et al., 2008), in Canada (Halfar et al., 2000), and in Greenland (Kamenos et al., 2012). These seasonal patterns in positional disorder and Mg-O bond strength underline the importance of either comparing high-Mg calcite that was deposited at the same time of year for different pCO2 treatments or allowing for the concentration of Mg present. Absence of significant differences in Mg concentration and Mg-O bond strength between growth pre-collection and during the control treatment are important as they exclude experimental handling impacts.
The Influence of pCO2 on Coralline Algal Structure
At both 750 and 1000 µatm pCO2, there was an increase in skeletal positional disorder and Mg-O bond strength in L. glaciale (Figs. 3 and 4). Although higher growth would be expected at high pCO2 in photosynthesizers, red coralline algae dissolve at night under high pCO2 and then hypercalcify during the day (Kamenos et al., 2013; Martin et al., 2013). Rapid hypercalcification likely leads to poor control over skeletal deposition resulting in greater positional disorder and thus Mg-O bond strength.
Despite their high-Mg calcite skeleton, a less stable polymorph of CaCO3 than calcite or aragonite, coralline algae appear to lower their Mg content at higher pCO2 (Fig. 3). This could be due to (1) preferential Mg2+ leaching, or (2) reduction of skeletally incorporated Mg2+ by the algae themselves, thereby reducing solubility and vulnerability to acidified conditions (Kamenos et al., 2013; Ries et al., 2009). Thus while hypercalcification to overcome dissolution indicates poor control over structural skeletal deposition, simultaneously reduced Mg 2+ content indicates either (1) increased active chemical control over their skeleton, or (2) reduced chemical skeletal control allowing Mg2+ leaching.
A single significant negative relationship between FWHM and pCO2 exists across calcite deposited in all seasons when allowing for Mg concentrations with a ±28 μatm standard error on pCO2 calculations (Table 1). Adjusting for Mg concentrations within the calcite skeleton is preferential to generation of season-specific relationships, as this (1) accounts for differences in inter-annual temperature causing a temporal offset in reconstructed pCO2, and (2) minimizes variability introduced by the within-growth band location of each analysis.
Six analytical sites per growth band were assessed in L. glaciale, fixing temporal sampling at two-month resolution. However, temperature reconstructions at two-week resolution are achievable from L. glaciale when using Mg paleothermometry (Kamenos et al., 2008). With suitable instrumental parameters, Raman laser spot size can be <10 µm indicating that pCO2 reconstructions at two-week resolution may also be possible.
Proxy Temporal Stability
In addition to skeletal Mg2+ reduction, OA-induced Mg-O bond strength changes may be enhanced with secondary environmental stressors, including temperature. Any historic changes in temperature will also have changed skeletal Mg concentrations (Halfar et al., 2000, Kamenos et al., 2008). This in turn affects Mg-O bond strength (Bischoff et al., 1985), as shown here at a seasonal scale (Figs. 3 and 4), further reducing skeletal reactivity to reduced pH during winter. This stresses the importance of incorporating Mg concentrations in reconstructions using Mg-O bond strength (e.g., Table 1). Similarly, any season-specific differences in Mg concentrations between pre-experimental and experimental growth not attributed to the experimental treatment are likely due to subtle site-specific differences between in situ (pre-experimental growth) and experimental temperatures in successive years.
Red coralline algae show significant potential to act as pCO2 proxies via use of their skeletal bonding strength. High-latitude species, including L. glaciale, are of particular importance in detecting historic changes in pCO2 enrichment as these species may experience the first pCO2 enrichment via OA due to high-latitude shoaling of the ΩCalcite (saturation state) depth (Feely et al., 2004). Moreover, there is a paucity of high-latitude shallow-water OA proxies in comparison to developments being made with equatorial and deep-water proxies including corals and foraminifera. We determined relationships between pCO2 and coralline algal skeletal Mg-O bond strength, a key step in understanding the capacity of molecular bonding strength to record pCO2. Instrumental costs for Raman are modest, sample preparation is minimal, and analytical times are fast. This provides a tool for reconstructing paleo-pCO2 which is not only a key carbonate chemistry parameter but also a critical parameter for understanding historic atmospheric CO2 concentrations.
We thank H. Stahl and N. Hicks for dissolved inorganic carbon analysis at the Scottish Association for Marine Science. Kamenos was funded by a Royal Society of Edinburgh Personal Research Fellowship (RES 48704/1) and Natural Environment Research Council (UK) grant NE/H017305/1. Pauly was funded by a Natural Sciences and Engineering Research Council of Canada Discovery Grant to E. LeDrew. Donohue was in receipt of a Marine Alliance for Science and Technology Ph.D. studentship. We thank the reviewers and editor (Ellen Thomas) whose comments improved the manuscript. This paper is a contribution to the UK Ocean Acidification Research Programme.
- Received 23 October 2014.
- Revision received 9 January 2015.
- Accepted 22 January 2015.
- © 2015 Geological Society of America