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Rapid Environmental Change over the Past Decade Revealed by Isotopic Analysis of the California Mussel in the Northeast Pacific

  • Catherine A. Pfister ,

    Affiliation Department of Ecology and Evolution, University of Chicago, Chicago, Illinois, United States of America

  • Sophie J. McCoy,

    Affiliation Department of Ecology and Evolution, University of Chicago, Chicago, Illinois, United States of America

  • J. Timothy Wootton,

    Affiliation Department of Ecology and Evolution, University of Chicago, Chicago, Illinois, United States of America

  • Pamela A. Martin,

    Affiliation Department of Geophysical Sciences, University of Chicago, Chicago, Illinois, United States of America

  • Albert S. Colman,

    Affiliation Department of Geophysical Sciences, University of Chicago, Chicago, Illinois, United States of America

  • David Archer

    Affiliation Department of Geophysical Sciences, University of Chicago, Chicago, Illinois, United States of America


The anthropogenic input of fossil fuel carbon into the atmosphere results in increased carbon dioxide (CO2) into the oceans, a process that lowers seawater pH, decreases alkalinity and can inhibit the production of shell material. Corrosive water has recently been documented in the northeast Pacific, along with a rapid decline in seawater pH over the past decade. A lack of instrumentation prior to the 1990s means that we have no indication whether these carbon cycle changes have precedence or are a response to recent anthropogenic CO2 inputs. We analyzed stable carbon and oxygen isotopes (δ13C, δ18O) of decade-old California mussel shells (Mytilus californianus) in the context of an instrumental seawater record of the same length. We further compared modern shells to shells from 1000 to 1340 years BP and from the 1960s to the present and show declines in the δ13C of modern shells that have no historical precedent. Our finding of decline in another shelled mollusk (limpet) and our extensive environmental data show that these δ13C declines are unexplained by changes to the coastal food web, upwelling regime, or local circulation. Our observed decline in shell δ13C parallels other signs of rapid changes to the nearshore carbon cycle in the Pacific, including a decline in pH that is an order of magnitude greater than predicted by an equilibrium response to rising atmospheric CO2, the presence of low pH water throughout the region, and a record of a similarly steep decline in δ13C in algae in the Gulf of Alaska. These unprecedented changes and the lack of a clear causal variable underscores the need for better quantifying carbon dynamics in nearshore environments.


Carbon dioxide-induced changes to the ocean carbon cycle have the potential to dramatically change the biology of the ocean [1]. There are several reports of precipitous declines in coastal seawater pH over the past 15 years [2], [3], [4], [5], but it is impossible to know whether these declines are anomalous or part of a natural fluctuation. The biological response will depend on whether organisms have experienced such pH levels in recent decades or centuries, as well as the rate of future change.

The chemical composition and growth patterns of shells of marine organisms can be used to infer the physical and chemical features of the ocean on both recent and paleontological time scales [6], [7], [8], [9]. Shells can provide proxy chemical records spanning longer time intervals than the instrumental record. The relative proportions of light (12C) and heavy (13C) stable isotopes of carbon (δ13C) in calcium carbonate-based shells can indicate carbon sources. Respiration of organic matter in subsurface ocean waters imprints intermediate and deep waters with isotopically light respired dissolved inorganic carbon (DIC), resulting in an inverse relationship between the intensity of upwelling and δ13C in the shell of the California mussel (Mytilus californianus) in southern California [6]. Shell material should also become less enriched in 13C due to inputs of isotopically lighter carbon from fossil fuel sources (the Suess effect: [10], [11]), lowering the relative abundance of 13C in atmospheric CO2 and surface ocean DIC through time. Stable isotope ratios of oxygen reflect water temperatures, with higher δ18O values indicating colder water [6], [9], [12], such as water upwelled from lower depths. Thus, carbon and oxygen isotopes of calcareous material are often used to reconstruct environmental data in the ocean [8].

Tatoosh Island (48.32°N, 124.74°W), 0.7 km off the northwestern tip of Washington State, USA, has been the site of extensive ecological investigation for five decades. Seawater data collected by a Hydrolab DataSonde (Hach Company, Loveland, CO) since 2000 show that the ocean at this site has undergone a sustained decline in pH over the past decade [2] at a rate that is an order of magnitude greater than expected based on model predictions [13] and the equilibrium response to rising atmospheric CO2 concentration. Field studies in the offshore waters of Washington [3] and throughout Puget Sound [4] have also found pH values in the surface ocean that were not anticipated for decades. At Tatoosh Island, there is no definitive explanation for the speed of this decline; aside from atmospheric CO2, there was little evidence for systematic changes in potential explanatory variables, including upwelling, chl a, temperature, salinity, and the Pacific Decadal Oscillation (PDO) [2]. Here we show that the shells of a cohort of mussels that recruited ∼30 m from the instrument in the year prior to its deployment preserved a record of a changing carbon cycle. Additionally, archival M. californianus shells exist due to the cadre of researchers that have studied at Tatoosh Island over the past several decades and also from the Makah tribe who have utilized the island for millennia [14]. We thus present isotopic analyses of historical shell sources from the same site spanning the past 1300 years, which demonstrate that recent carbon isotopic compositions of shells are historically unprecedented.


The modern M. californianus shells from Tatoosh Island were aged as far back as 1999 providing historical material for as much as 11 years per individual. The archival shell material spans from the 1960s through 1990, while midden shells were dated back to 663–1008 AD, dates consistent with previous estimates of human occupation [14]. The δ13C values (PDB scale) ranged from −1.13 to 1.17 ‰ from 663 A.D. until 2009. The mean value of δ13C has declined into the present with a decrease of 0.36 ‰ from the midden to the archival shells and an additional 0.53 ‰ decline for δ13C in modern shells (Figure 1a, ANOVA and Tukey HSD, F2,289 = 81.32, p<0.001). The δ18O of M. californianus showed a different pattern, with midden and modern shells having similar means, while the archival shells had a lower mean δ18O (Fig 2a, ANOVA and Tukey HSD, F2,289 = 11.77, p<0.001), perhaps recording warming during the 1983–1984 ENSO event. We further verified that the shells record oceanic events by using the Kim and O'Neil equation [15] modified by Ford [9] to predict seawater temperature from our modern shell material. Using our measured δ18O at Tatoosh in 2009 (−0.50‰, n = 17 from May to August) and 2010 (−0.87‰, n = 20), all modern shell δ18O values generated a range of temperatures from 5.9 to 14.0°C, with a mean of 10.4 and 8.8 using 2009 and 2010 δ18O measurements, and were thus were highly comparable to our mean measured seawater temperatures (Table 1).

Figure 1. The δ13C for inner shell material of M. californianus from Tatoosh Island.

a. The δ13C (‰, PDB scale) for inner shell material from 663 to 2009 AD. The data are divided into Native American midden shells (black, n = 11), archival shells (red) collected ∼1975 (n = 5), 1986 (n = 7), 1990 (n = 3), and modern shells (blue) collected in 2009 and 2010 (n = 56). Note that the archival shells from the 1970s do not have an exact collection year; we have assigned them 1975. Means for each of these 3 groups are shown with standard error bars. Inset figure shows the relationship between δ13C and age (in years) using a linear mixed effects model for each of the 3 shell groupings. There was no relationship between δ13C and mussel age for archival shells (coefficient = 0.003 ‰ yr−1, df = 49, p = 0.823) while midden mussels showed a positive relationship (0.064 ‰ yr−1, df = 38, p = 0.041). b. An expanded scale for the relationship between δ13C and year for modern shells only with small, young shells (38.8–52.6, n = 9) designated with a “o”. A linear mixed effects model estimated a significant negative slope of −0.071 ‰ yr−1 (se = 0.011, df = 85, p<0.001).

Figure 2. The δ18O for inner shell material of the same M. californianus from Tatoosh Island.

a. The δ18O (‰, PDB scale) for inner shell material from 663 to 2009 AD with shells as shown in Fig 1. Figure key is identical to Fig 1. b. An expanded scale for archival and modern shells. The slope of δ18O with year for modern shells is not significant (0.006 ‰ yr−1, se = 0.008, df = 85, p = 0.469).

Table 1. The isotopes of Carbon and Oxygen (‰, PDB scale) in the shells of M. californianus and environmental variables at Tatoosh and vicinity as a yearly average.

Patterns and Environmental Correlates in Modern Mussels

The δ13C of modern shells at Tatoosh declined significantly at a rate of −0.071 ‰ yr−1 over an 11-year period (Figure 1b, linear mixed effects model, se = .011, n = 53, df = 85, p<0.001). Although mussels were collected from 4 sites on Tatoosh in 2009, site was not a significant explanatory variable for δ13C measurements (Likelihood ratio Test, χ12 = 2.8, p = 0.10) We also found no effect of shell age on δ13C when we compared the δ13C in 2007 and 2008 for large (129.3 – 158.0 mm length) versus small (38.8–52.6 mm, n = 9) mussels collected in 2009 (ANOVA, p = 0.547, Fig 1b). In contrast to δ13C, there was no systematic change in the δ18O from these same modern M. californianus shells, although the mean differed among years (Fig 2b, linear model, slope = 0.006, se = 0.008, df = 85, p = 0.469). As with δ13C, there was no effect of mussel size (small vs large) on the mean δ18O (ANOVA, p = 0.091, Fig 2b). The M. californianus collected by E. Sanford in August 2001 were 2–3 years old and thus extended back only to 1999, overlapping with our decade-old shells collected in 2009. Although they did not allow us to extend an archival record prior to 1999, they further demonstrated concordance with our 2009 shells; there were no differences in the δ13C values in 1999, 2000, and 2001 (p = 0.839) nor with δ18O values (p = 0.288) with these shells of different ages. The inclusion of these 2001 shells negligibly affected our estimates of δ13C with year, resulting in a slope of −0.069 vs −0.071 ‰ yr−1 without these 2001 shells.

Carbon and oxygen isotopes of mussels showed some strong relationships with environmental data. The δ13C of mussels exhibited a significant negative relationship with the annually averaged upwelling index (UI) and a significant positive relationship (and the lowest AIC scores) with seawater pH and atmospheric CO2 (Table 2) when these variables were tested independently. A linear mixed effect model using these three independently significant variables to explain the decline in δ13C was favored in model selection over any single variable model with a Likelihood Ratio Test (130.4 vs 139.8–147.6, Table 2) and thus strongly suggests that shells are responsive to carbon chemistry. All other environmental variables tested, including the UI (from April to September only), the PDO, silicate, nitrate and the seawater temperature at Tatoosh, were not associated with shell δ13C (Table 2).

Table 2. The results of linear mixed effects models testing explanatory variables for carbon and oxygen isotopes in Mytilus californianus.

The PDO, calculated as either an annual average or averaged from April to September, was the only variable associated with the δ18O of mussels, showing a consistent negative relationship. The lower δ18O values in the archival shells may reflect the timing of the 1983/84 ENSO event, where surface temperatures warmed when upwelling weakened [16]. No significant variation in the δ18O of M. californianus shells was explained by salinity, seawater temperature, or the UI (Table 2). The lack of correlation with local mean annual temperature or salinity might arise because our instrumental data are not year-round, as is the PDO. Salinity also varies relatively little at Tatoosh on an interannual basis. The stronger correlation of both the UI and PDO with δ13C and δ18O when averaged over the entire year, rather than only April to September, suggest that there is continuous shell growth and that conditions over the entire year are recorded in the shell.

Patterns in Archival and Midden Mussels

The δ13C values of archival and midden M. californianus were significantly higher than modern shells and showed no evidence of the declining trend in δ13C that characterized modern shells. Over the 14 individual mussels we analyzed spanning this period, the coefficient for an effect of year (0.006 ‰ yr−1) did not differ significantly from 0 (df = 49, p = 0.538) and was positive. The 11 M. californianus shells from Native American middens on Tatoosh also showed no significant year trend for δ13C (−0.001 ‰ yr−1, df = 38, p = 0.354). However, in the case of midden shells, the time span is several centuries. We thus also analyzed shells for a pattern and found a positive relationship (0.064 ‰ yr−1, df = 38, p = 0.041). Thus, the pattern of declining δ13C over the past decade at Tatoosh Island has not been observed at any other time over past decades and centuries.

The pattern at Tatoosh was also observed at another locale 85 km inside the Strait of Juan de Fuca at Observatory Point, WA (48.264°N, 124.248°W). Although the Observatory Point mussels were not as old as the modern Tatoosh mussels, with a record extending only to 2002, the shell δ13C values did not differ from those at Tatoosh from 2002−2008 (ANOVA, slope = −0.037 ‰ yr−1 (se = 0.034), site effect: p =  0.224, site by year interaction: p = 0.614). There was also no difference in the δ18O pattern through time between these two sites (ANOVA, site effect: p = 0.967).


The rate of decline in mussel shell δ13C from 1999−2009 was faster than can be explained by equilibration with the rising CO2 concentration of the atmosphere and the increasing contribution of isotopically light fossil fuel carbon (the Suess effect). The relationship between δ13C in atmospheric CO2 and the amount of CO2 in the atmosphere, δ13C  =  −0.0147[CO2]-2.60, predicts a δ13C rate of change of −0.0282 ‰ yr−1 [17], assuming rapid equilibration between the surface ocean and the atmosphere. Other calculations for seawater DIC estimate a global ocean average decline of −0.015 ‰ yr−1 in δ13CDIC [18]. Both are much less than our observed decline in δ13C of −0.071 ‰ yr−1; the observed shell δ13C decline is consistent in sign with the observed 10-year decline in pH at Tatoosh Island [2], although the pH decrease was even greater, over 13 times stronger than can be explained by equilibrium with the rising atmospheric CO2 over this time period. The carbon chemistry of the surface waters is thus changing much more quickly than can be explained by simple immediate forcing from atmospheric CO2.

Hypotheses for the Rapid δ13C Decline in Mussel Shells

We address three hypotheses for the shell δ13C decline that is 2.5 times greater than expected based on atmospheric CO2 levels and the assumption that atmospheric CO2 is in equilibrium with the pCO2 of the surface ocean (e.g. [19]). First, the food web has shifted from a carbon source that is heavier to one that is lighter, a possibility if phytoplankton has replaced kelp and benthic microalgae as a carbon source for mussels (e.g. [20]). Second, the animals are using increasing amounts of 13C depleted metabolic CO2. Third, factors affecting biological production may have changed. Specifically, an increase in upwelling would result in an increase in nutrient-rich, 13C-depleted seawater and would be consistent with our declining shell δ13C. Alternatively, increased respiration and decreased phytoplankton abundance could also contribute to the observed decline in shell δ13C.

A change to the food web from dominance by isotopically heavier benthic algae to lighter phytoplankton could result in a pattern of decline in δ13C of filter-feeding species such as mussels. Because algal δ13C can differ by an order of magnitude more than the shell changes we saw, it would be possible to see shifts in the shell signature with relatively small dietary changes. However, such a shift would not affect benthic grazers such as the limpet Lottia pelta, as their diets are restricted to benthic microalgae. The significant decline in the δ13C of limpets over the three time points provides evidence counter to a food web shift hypothesis (Fig 3a, linear mixed effects model, time coefficient = −0.206, p = 0.009, n = 5). Although a slope coefficient of −0.206‰ yr−1 is greater than that of M. californianus, the time interval (and thus units) for that slope is uncertain because annual bands are not always distinct on L. pelta and the slope thus represents only a relative change among three layers. The δ13C of archival shells from the 1970s and 1980s (n = 7) were significantly greater than shells collected in 2009 (n = 10) (mean±se = 1.56 ‰ ±0.16 vs 1.02‰ ±0.16, F1,15 = 5.102, p = 0.039). When we used known years in all L. pelta collections by examining only the most recently produced shell layer, we estimated a slope of −0.023 ‰ yr−1 from ∼1974 to 2009 (p = 0.064, n = 13). The concordance in the decline of both mussel and limpet shell δ13C suggest that the causal process driving a decline in shell δ13C is unrelated to trophic mode. Further, the relatively small offset between our shell δ13C with that of seawater in the surface ocean (δ13CDIC  = 1.8 to 2.2 ‰ at Station P of the northeast Pacific (18)) suggests that shells reflect inorganic carbon in the water and that food web effects of highly depleted values for macroalgal versus phytoplankton [20] are unlikely to differentially affect shell values.

Figure 3. The δ13C (‰, PDB scale) of limpets (Lottia pelta) at Tatoosh Island.

a. The δ13C of limpets collected in 2009 (n = 5) showed a significant decline among the 3 sample chronologies (−0.206 ‰ yr−1, p = 0.009), b. Archival and modern L. pelta δ13C values where year could be assigned with certainty, had a coefficient of −0.023 ‰ yr−1 (p = 0.063, n = 13) .

Although a decline in modern bivalve shell δ13C has been shown to be related to increased use of metabolic CO2 with age [21], [22], neither our midden nor archival mussel shells showed a decline related to age (Fig 1a), nor did shell of different aged individuals laid down in the same year differ in the δ13C (Fig 1b). Furthermore, we found no relationship between δ13C and δ18O (linear mixed effect model, coefficient  = −0.012, df = 82, p = 0.925) when we structured the analysis by individual, a result that might have indicated metabolic effects on carbon and oxygen isotopes (e.g. [23]). Thus, even though mussels may not be precipitating calcium carbonate in equilibrium with seawater [6], we cannot yet identify a metabolic process that is causing a δ13C decline through time in modern shells.

Changes to δ13C could be due to factors affecting biological production, either via changes to upwelling or related changes to productivity. Increased upwelling results in decreased seawater δ13C as a result of the oxidation of biological material that is isotopically light. Other studies of plant and animal tissue have attributed declines in δ13C that are greater than the expected based on the Seuss effect to upwelling [11], [24]; however, upwelling has not been rigorously tested. Several sources of data test the hypothesis that upwelling increased in the region, resulting in declining δ13C. We found a linear positive trend in the daily UI from 1998 through 2009 for 48°N, with a slope of 0.0109 (p<0.001, r2 = 0.016, Figure S1). When we analyzed the spring and summer period when upwelling occurs (April through September), there is no increasing trend (−0.0001, p = 0.884); the positive trend comes from an analysis of October through March only (0.021, r2 = 0.039, p<0.001) when downwelling occurs. Thus, it appears that it is not stronger upwelling during the season when positive values for the Upwelling Index prevail, but rather a weakening of downwelling typical of fall and winter months.

If net upwelling has increased, nitrate and soluble reactive phosphorus (henceforth “phosphate”) levels should increase as well. The concentrations of nitrate and phosphate have a known empirical relationship with δ13C at 42oN in the northeast Pacific, following Redfield ratios for both nitrate and phosphate [25]. We thus assumed a Redfield ratio and estimated whether increasing nutrients associated with upwelling can corroborate the decline in δ13C. Using annually averaged water nutrient data from Tatoosh, we found no statistically significant temporal trends in nitrate and phosphate (nitrate: F = 1.20, p = 0.302, slope = 0.312 µM yr−1; phosphate: F = 0.50, p = 0.497, slope = 0.019 µM yr−1, Table 1). Nonetheless, one can use these slopes to explore how nutrient changes might have affected δ13C. If we assume that the relationship between nitrate and phosphate through time was significantly different from zero, and used our estimated coefficients, δ13C is predicted to decrease 0.019 and 0.018 ‰ yr−1 due to increasing nitrate and phosphate, respectively, an amount that still does not explain the observed decline. A 7.13 µmol/kg mean change in nitrate over the study period (or 0.446 µmol/kg mean change in phosphate) is required to explain the decreasing δ13C, a change in nitrate that is not supported by our data.

We further hypothesized that any circulation pattern that might change the supply of CO2 in shallow waters would be revealed by temporal trends in seawater temperature surrounding Tatoosh Island. Because Tatoosh temperature is only recorded from April to September, we used Cape Elizabeth Buoy (NDBC Buoy 46041, for mean daily sea surface temperature (SST, °C). We found a linear negative trend in SST of −0.0002 per year from 1998 through 2009 showing temperatures declining over the past decade (Figure S2, p<0.001, r2 = 0.014). Although this buoy is 50 km to the southwest of Tatoosh and records SSTs several degrees higher than Tatoosh, it still serves as an indicator of relative temperature in the region [26].

Changes in the upwelling or circulation regimes could affect dissolved oxygen (DO) in these regions [4], [27]. Decreases through time in DO might indicate increased oxidation of organic matter and thus the increased release of relatively 13C depleted CO2. Although the DO probe was not functional at all times and all years at Tatoosh (Table 1), there were still 6 years of data spanning 2000 to 2009. The mean daily DO showed a positive linear trend with time (slope = 0.0008, p<0.001, r2 = 0.222, df  = 18304), not the negative trend that is needed to explain a declining δ13C associated with water influenced by high respiration.

A final possibility for the decline in δ13C due to biological production changes is phytoplankton decline and thus a reduced uptake of CO2, a hypothesis that had no support from remote sensing data that estimates chl a as a proxy for phytoplankton concentration (SeaWiFS (1998–2007) and MODIS data (Aqua MODIS years: 2000–2009, For SeaWiFS the monthly mean of chl a (mg m−3) of 5, 0.1 degree gridded areas around Tatoosh from 1998 to 2007 showed no linear change through time (Fig S3, slope  = −.073, p = 0.622, r2 = 0), a result paralleled by Aqua MODIS data on chl fluorescence (Fig S4, −0.0005, p = 0.487, r2 = 0). Thus, although there is some indication of global declines in phytoplankton [28], there was no indication of this pattern in the area surrounding Tatoosh.

Finally, we note that the equilibration time of the δ13C of seawater is about 10 times longer than that of pCO2, potentially decoupling the δ13C of DIC from surface ocean nutrient and pCO2 values. Sea surface δ13C increases with latitude [29], so the observed decrease in the shell δ13C may in part be attributable to increased influence of lower-latitude water over time, as previously suggested by Ortiz et al [25]. Additionally, decreasing shell δ13C at Tatoosh Island is consistent with upwelling of younger water, as if fossil fuel CO2 were invading the coastal waters both from the atmosphere and, increasingly, through the thermocline. However, the magnitude of the δ13C change recorded in mussel shells (−0.71 ‰ per decade) is much greater than the observed 0.15 ‰ per decade decrease for global ocean seawater [18] suggesting this cannot be a sole mechanism. Thus, despite the number of hypotheses we were able to test (Table 3), we can only speculate about sources of seawater with lower δ13C DIC. However, our analyses highlight the need for increased research efforts on the carbon cycle in nearshore environments (Table 3), including δ13C and DIC sampling, and attention to biological and circulation changes in nearshore environments.

Table 3. The hypothesized drivers of a declining δ13C in the California mussel, our hypothesis testing, and suggested further research.


In sum, we found no evidence that a single factor accounts for the rapid decline that we observed in δ13C of M. californianus shells. Although atmospheric CO2 explains a slope of −0.028 ‰ yr−1, the remaining changes seems unrelated to the type of carbon available to filter feeders. Environmental variables that might have contributed to declining shell δ13C over the past decade included an increase in upwelling and a possible increase in nitrate and phosphate. However, these changes are slight and unable to account for a slope 0.043‰ per year lower than expected based on calculations using atmospheric CO2 concentrations. Upwelling, for example, is increasing only 0.0109 units per year over the past decade - a change that seems inconsequential given that the UI can range over hundreds of units over several days. Similarly, the nitrate and phosphate increases that would have to be inferred over this interval to have so greatly affected δ13C (7.13 and 0.446 µmol/kg, respectively) have not been observed in this area.

Our observed decline in shell δ13C parallels other signs of rapid changes to the nearshore carbon cycle in the northeast Pacific, including a decline in pH that is an order of magnitude greater than predicted by an equilibrium response to the rising CO2 concentration of the atmosphere [2], the presence of low pH water throughout the region [3], [4], and a record of a similarly steep decline in δ13C of algal calcium carbonate in the Gulf of Alaska [11]. Whether the decline we report can be attributed to single factors such as circulation changes that have not yet been documented, a fundamental difference in the cycling of carbon in this region, an alteration of carbon metabolism in these animals, perhaps via an effect of changing seawater carbon chemistry on shell composition (e.g. [8]), or undescribed interactions among these factors is unknown. Mussel shells, however, indicate that these changes are unprecedented and the lack of a clear causal variable underscores the need for better quantifying carbon dynamics in nearshore environments.

Materials and Methods

In April of 2009 24 of the largest M. californianus were collected in the mid intertidal (tidal height ∼0.6–1.0 m above MLLW) in the area of Tatoosh Island, WA known as Hedophyllum Cove, where they recruited in 1999 and 2000 [30], approximately coincident with our instrument deployment in the same locale. An additional 9 small mussels (38.8–52.6 mm) were also collected to test whether younger mussels had similar isotopic values for a given year. We also collected 3 of the largest M. californianus we could find on Tatoosh in 2009, at a site known as the Glacier on Tatoosh and 8 of the largest shells from the Finger site and 3 from the Main Beach of Tatoosh. In April 2010, we collected 7 more of the largest available animals from Hedophyllum Cove to sample only in the 2009 growth area. To test whether mussels from a site 85 km east in the Strait of Juan de Fuca showed similar isotopic ratios of carbon and oxygen to Tatoosh, 10 of the largest shells from the mid intertidal of Observatory Point (48.264°N, 124.248°W) were collected coincident with the April 2009 collection on Tatoosh.

To prepare the shells for isotope sampling, we removed all soft parts and epiphytes from the shells and dried them at 40°C. Our methods were based on Schöne et al. [31] where shells were cleaned in a 5% bleach solution for 1h, then rinsed three times in MilliQ water for 15 min. The length, height and width of each shell was measured, then we sectioned one valve of each individual lengthwise along its axis of maximum growth by first reinforcing with epoxy (JB QuikWeld, Sulphur Springs, TX), then sawing with a Isomet™ Low Speed Saw and diamond edge cutting blades (Buehler Co.). We prepared a cross sectional slide (1.5 mm width) along the axis of maximum growth. We polished the slides using a 600 grit silicon carbide powder (Buehler Co.) followed by a microcloth with 3 µm diamond polishing suspension (MetaDi Polycrystalline Diamond Suspension, Buehler Co.) to better visualize the annual bands. M. californianus deposits calcitic shell in annual layers with the newest shell material deposited in proximity to the inner soft tissue of the animal. Our analyses focused on the calcitic inner prismatic layers [32]; mussels were aged by counting the number of these bands designating the band closest to the mantle as the most recent. The fact that the Hedophyllum Cove shells showed ∼10 annual bands and were known to have recruited in 1999 [30] gave us confidence in our aging method. Shell material was collected by drilling in the center of each growth band in each individual using a Dental Rotary drill (Brasseler USA). Because we knew the date of shell collection, we were able to assign growth increments to particular years. Shell material was analyzed for stable isotopes of carbon (δ13C) and oxygen (δ18O) in the Earth Systems History Laboratory at Brown University (Providence, RI).

Sources of archival shells included 9 shells collected in 1986, 1987, 1990 from Oystercatcher (Haematopus bachmani) middens (JTW), 8 shells collected by E. Sanford in August 2001 at north-facing part of Tatoosh, and 5 shells collected by T. Suchanek in the 1970s. The precise date of collection of the shells is not known, though we placed the collection date at 1975 in the midst of the time that Suchanek was studying mussels on Tatoosh. Tatoosh was a Native American summer camp for the Makah for centuries prior to occupation by the US Coast Guard and Navy in the 1800s. Middens have been excavated on the island [14] and we obtained 11 M. californianus valves from the Makah Cultural and Resource Center. The midden shells were prepared with identical methodology except that the entire valve was encased in epoxy prior to sawing to protect these older shells from breakage. Shell ages were obtained from NOSAMS ( via radiocarbon dating by sampling each shell individually in the last complete annual growth band recorded by the animal.

The limpet, Lottia pelta, is an abundant benthic grazer in the rocky intertidal of the northeast Pacific. Limpets add new calcium carbonate throughout the interior of the shell, and grow from the apex outward; hence, the apex provides the longest time series of calcium carbonate deposition. Limpets (Lottia pelta) were collected at several sites on Tatoosh in 2009; archival specimens were from oystercatcher middens described above (1986, 1987, 1990), while a single individual came from the 1970s collection of Suchanek. We sectioned limpets through the apex using the methods described above. Because limpets erode at the apex, limpets did not provide sufficiently high resolution for annual sampling. Instead, the apex was sampled in presumed time horizons of the most recent year of growth, and back through time for a midpoint and an ‘oldest’ horizon. We thus only used limpets for a relative trend in isotopic signature and only assigned the most recent growth strata to a particular year.

Instrumental data on seawater temperature, salinity, pH, dissolved oxygen, and chl a have been recorded every 30 min during the spring and summer months since 2000 at Tatoosh Island. Detailed methods on this collection have been described [2], and have continued through the period of growth recorded by the M. californianus shells. We have also measured water nutrients (nitrate, nitrite, ammonium, soluble reactive phosphorus, silicate) monthly at 10 locales around Tatoosh Island from April to September since 1998.

Environmental variables estimated over larger spatial and temporal scales included the upwelling index (UI) for 48°N, 125°W (, an indicator of upwelling strength based on wind stress measurements, as well as the Pacific Decadal Oscillation (PDO,, a composite indicator of ocean temperature anomalies [33], seawater temperature from Buoy 46041 ∼50 km to the southwest from Tatoosh (, and remote sensing of chl a (SeaWiFS, AquaModis).

Isotopes of carbon and oxygen were sampled on an annual time scale while all environmental data was finer-grained, ranging from half-hourly to monthly. We thus aggregated environmental data, estimating annual means for our instrumental data that spanned April to September. For the UI and PDO we averaged both over the entire year or using only the April to September period corresponding to our measurements. These data groupings represented two different growth models for these molluscs – one where they grew year-round, and another where the principal growing season for M. californianus is the spring and summer (e.g. [34]). In testing for relationships among environmental factors and δ13C and δ18O, the plethora of variables would have compromised our degrees of freedom. We thus structured our analyses to focus on those factors that are known to have a relationship to each element, tested their relationship in isolation, and then used a multi-effect model where warranted. Our statistical analyses recognized the structure of data, where individuals are sampled multiple times and thus may impart a correlation structure on the data. We thus treated shell identity as a random effect in mixed effect models when analyzing time trends and relationships with environmental variables. All statistics were done with R (

We obtained the necessary permits for acquiring shells including a permit from the Makah Tribal Nation (for Tatoosh collections) and Washington Department of Fish and Wildlife shellfishing permit for collections at Observatory Point.

Supporting Information

Figure S1.

Daily Upwelling Index (UI) in proximity to Tatoosh Island (48°N) from 1998–2009. The UI showed a significant positive linear trend (slope = 0.0109, p<0.001), though the r2 was low (r2 = 0.016).


Figure S2.

Mean daily SST for Buoy 46041 (Cape Elizabeth) in °C from 1998–2009. The SST showed a significant negative trend (slope = −0.0002, p<0.001), though the r2 was low (r2 = 0.014).


Figure S3.

Mean monthly SeaWiFS values from 1998–2007 (chl a in mg m−3). There was no significant pattern for SeaWiFS with time (−0.073, p = 0.622).


Figure S4.

Mean monthly Aqua MODIS chl fluorescence data from 2000–2009. There was no significant pattern for AquaMODIS data with time (−0.0005, p = 0.487).



We thank researchers who loaned us mussel shells, including T. Suchanek and E. Sanford, those who helped prepare the mussels (A. Barner and B. Colson), and R.T. Paine for pointing out the Tatoosh mussel cohort. We are grateful to the Makah Tribal Nation for the access to the study areas and the use of midden shells, with special thanks to the expertise of J. Bowechop and G. Wesson. The Pfaffs kindly allowed access across their property. We thank C. Belanger for methodological advice and S. Clemens for providing the isotope data.

Author Contributions

Conceived and designed the experiments: CAP SJM JTW PAM ASC. Performed the experiments: CAP SJM JTW. Analyzed the data: CAP SJM JTW DA. Contributed reagents/materials/analysis tools: CAP JTW PAM. Wrote the paper: CAP SJM JTW ASC DA.


  1. 1. Doney C, Fabry VJ, Feely RA, Kleypas JA (2009) Ocean acidification: the other CO2 problem. Ann Rev Mar Sci 1: 169–192.
  2. 2. Wootton JT, Pfister CA, Forrester JD (2008) Dynamic patterns and ecological impacts of declining ocean pH in a high-resolution multi-year dataset. Proc Natl Acad Sci 105: 18848–18853.
  3. 3. Feely RA, Sabine CL, Hernandez-Ayon JM, Ianson D, Hales B (2008) Evidence for upwelling of corrosive “acidified” water onto the continental shelf. Sciencexpress. 10.1126/science.1155676.
  4. 4. Feely RA, Alin SR, Newton J, Sabine CL, Warner M, et al. (2010) The combined effects of ocean acidification, mixing, and respiration on pH and carbonate saturation in an urbanized estuary. Estuar Coast Shelf Sci 88: 442–449.
  5. 5. Provoost P, van Heuven S, Soetaert K, Laane RWPM, Middelburg JJ (2010) Seasonal and long-term changes in pH in the Dutch coastal zone. Biogeosciences 7: 3869–3878.
  6. 6. Killingley JS, Berger WH (1979) Stable isotopes in a mollusk shell: detection of upwelling events. Science 205: 186–188.
  7. 7. Klein RT, Kyger C, Lohmann KC, Thayer CW (1996) Bivalve skeletons record sea-surface temperature and delta 18O via Mg/Ca and 18O/16O ratios. Geology 24: 415–418.
  8. 8. Spero J, Bijma J, Lea DW, Bemis BE (1997) Effect of seawater carbonate concentration on foraminiferal carbon and oxygen isotopes. Nature 390: 497–500.
  9. 9. Ford HL, Schellenberg SA, Becker BJ, Deutschman DJ, Dyck KA, et al. (2010) Evaluating the skeletal chemistry of Mytilus californianus as a temperature proxy: effects of microenvironment and ontogeny. Paleoeceanography 25: PA1203.
  10. 10. Druffel ERM, Benavides LM (1986) Input of excess CO2 to the surface ocean based on 13C/12C ratios in a banded Jamaican sclerosponge. Nature 321: 58–61.
  11. 11. Williams BJ, Halfar J, Steneck RS, Wortmann UG, Hetzinger S, et al. (2011) Twentieth century δ13C variability in surface water dissolved inorganic carbon recorded by coralline algae in the northern North Pacific Ocean and the Bering Sea. Biogeosciences 8: 165–174.
  12. 12. Ullmann CV, Wiechert U, Korte C (2010) Oxygen isotope fluctuations in a modern North Sea oyster (Crassostrea gigas) compared with annual variations in seawater temperature: Implications for palaeoclimate studies. Chem Geol 277: 160–166.
  13. 13. Orr JC, Fabry VJ, Aumont O, Bopp L, Doney SC, et al. (2005) Anthropogenic ocean acidification over the twenty-first century and its impact on calcifying organisms. Nature 437: 681–686.
  14. 14. McMillan AD (1999) Since the Time of the Transformers: The Ancient Heritage of the Nuu-chah-nulth, Ditidaht and Makah. Vancouver, British Columbia: UBC Press.
  15. 15. Kim ST, O'Neil JR (1997) Equilibrium and non-equilibrium oxygen isotope effects in synthetic carbonates. Geochim Cosmochim Act 61: 3461–3475.
  16. 16. Cane MA (1983) Oceanographic events during El Niño. Science 2222: 1189–1195.
  17. 17. Quay P, Tilbrook B, Wong C (1992) Oceanic uptake of fossil fuel CO2: Carbon-13 evidence. Science 256: 74–79.
  18. 18. Sonnerup RE, Quay PD, McNichol AP, Bullister JP, Westby TA, et al. (1999) Reconstructing the oceanic 13C effect. Global Biogeochemical Cycles 13: 857–872.
  19. 19. Takahashi T, Sutherland SC, Wanninkhof R, Sweeney C, Feely RA, et al. (2009) Climatological mean and decadal change in surface ocean pCO2, and net sea-air CO2 flux over the global oceans. Deep-Sea Research Part II: Topical Studies in Oceanography 56: 554–577.
  20. 20. Duggins DO, Simenstad CA, Estes JA (1989) Magnification of secondary production by kelp detritus in coastal marine ecosystems. Science 245: 170–173.
  21. 21. Lorrain A, Paulet Y-M, Chauvaud L, Dunbar RB, Mucciarone DA, et al. (2004) δ13C variation in scallop shells: increasing metabolic contribution with body size? Geochim Cosmochim Acta 68: 3509–3519.
  22. 22. Gillikin DP, Lorrain A, Meng L, Dehairs F (2007) A large metabolic carbon contribution to the δ13C record in marine aragonitic bivalve shells. Geochim Cosmochim Acta 71: 2936–2946.
  23. 23. McConnaughey TA, Gillikin DP (1989) Carbon isotopes in mollusk shell carbonates. Geo-Mar Lett 28: 287–299.
  24. 24. Schell D (2001) Carbon isotope ratio variations in Bering Sea biota: the role of anthropogenic carbon dioxide. Limnol Oceanogr 46: 999–1000.
  25. 25. Ortiz JD, Mix AC, Wheeler PA, Key RM (2000) Anthropogenic CO2 invasion into the northeast Pacific based on concurrent δ13CDIC and nutrient profiles from the California Current. Global Biogeochem Cycles 14: 917–929.
  26. 26. Pfister CA, Wootton JT, Neufeld C (2007) The relative roles of coastal and oceanic processes in determining physical and chemical characteristics of an intensively sampled nearshore system. Limnol Oceanogr 52: 1767–1775.
  27. 27. Chan F, Barth JA, Lubchenco J, Kirincich A, Weeks H, et al. (2008) Emergence of anoxia in the California Current large marine ecosystem. Science 319: 920.
  28. 28. Boyce DG, Lewis MR, Worm B (2010) Global phytoplankton decline over the past century. Nature 466: 591–596.
  29. 29. Gruber N, Keeling CD, Bacastow RB, Guenther PR, Lueker TJ, et al. (1999) Spatiotemporal patterns of carbon-13 in the global surface oceans and the oceanic Seuss effect. Global Biogeochem Cycles 13: 307–33.
  30. 30. Paine RT, Trimble AC (2004) Abrupt community change on a rocky shore – biological mechanisms contributing to the potential formation of an alternative state. Ecol Lett 7: 441–445.
  31. 31. Schöne BJ, Fiebig J, Pfeiffer M, Gleß R, Hickson J, et al. (2005) Climate records from a bivalved Methuselah (Arctica islandica, Mollusca; Iceland). Paleogeog Paleoclim Paleoecol 228: 130–148.
  32. 32. Dodd JR (1964) Environmentally controlled variation in the shell structure of a pelecypod species. J Paleont 38: 1065–1071.
  33. 33. Mantua N, Hare SR, Zhang Y, Wallace JM, Francis RC (1997) A Pacific interdecadal climate oscillation with impacts on salmon production. Bull Amer Meteorol Soc 78: 1069–1079.
  34. 34. Coe WR, Fox DL (1944) Biology of the California sea-mussel (Mytilus californianus) III. Environmental conditions and rate of growth. Biol Bull 87: 59–72.