INTRODUCTION
Natural disasters such as tsunamis, earthquakes, typhoons, and volcanic ash falls can substantially disturb benthic ecosystems in coastal areas (López et al. Reference López, Penchaszadeh and Marcomini2008; Jaramillo et al. Reference Jaramillo, Dugan, Hubbard, Melnick, Manzano, Duarte, Campos and Sanchez2012; Seike et al. Reference Seike, Shirai and Kogure2013; Harris Reference Harris2014). In particular, tsunamis can cause either rapid sedimentation, thus burying benthic organisms deep under the seafloor, or rapid erosion, thus washing them out of the upper layer of substrate and exposing them to predation (Kranz Reference Kranz1974; Bromley Reference Bromley1996; López et al. Reference López, Penchaszadeh and Marcomini2008). On 11 March 2011, the Tohoku-Oki Earthquake, a M9.0 megathrust earthquake, ruptured the plate boundary off the Pacific coast of northeastern Japan (Ide et al. Reference Ide, Baltay and Beroza2011) and generated a huge tsunami that affected 2000 km of the Pacific coast of northeastern Japan (Mori et al. Reference Mori, Takahashi, Yasuda and Yanagisawa2011). In Funakoshi Bay, Iwate prefecture, the tsunami run-up height was 29.4 m (Ishimura and Yamada Reference Ishimura and Yamada2019), and large-scale seafloor erosion and sedimentation occurred, followed by the re-establishment of bioturbation (Seike et al. Reference Seike, Kitahashi and Noguchi2016, Reference Seike, Shirai and Kubota2017, Reference Seike, Sassa, Shirai and Kubota2018, Reference Seike, Sassa, Shirai and Kubota2019). Furthermore, population densities of sand dollar Scaphechinus mirabilis (an echinoid) and Sakhalin surf clam Pseudocardium sachalinense (a mollusk) in the bay were significantly decreased by the tsunami disturbance (Seike et al. Reference Seike, Shirai and Kogure2013). Although investigating the population dynamics of animals with a large population density before (and after) the tsunami is possible if the data from before the event are available, investigating those with a small population density and rare catch opportunity is extremely difficult. In addition, in most coastal areas, environmental or ecosystem survey records from before an event are unlikely to be available; as a result, it is usually very difficult or even impossible to assess the effect of a catastrophic event on coastal ecosystems. Some marine animals such as mollusks have a countinuously grown calcium carbonate shell. As a result, mollusk shells continuously record the ambient environment, making them excellent archives of past environments and environmental disturbances (e.g., Murakami-Sugihara et al. Reference Murakami-Sugihara, Shirai, Hori, Amano, Fukuda, Obata, Tanaka, Mizukawa, Sano and Takada2019). The cold-water venerid bivalve Mercenaria stimpsoni (Stimpson’s hard clam), which lives in Funakoshi Bay, is a long-lived mollusk with a shell that displays distinct annual growth increments (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Hori and Tanabe2017, Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a; Shirai et al. Reference Shirai, Kubota, Murakami-Sugihara, Seike, Hakozaki and Tanabe2018). It is thus possible to test the response of this marine mollusk to environmental perturbation, despite its low population density in the bay (Seike et al. Reference Seike, Shirai and Kogure2013), because gaps in the shell record can be filled by using crossdating to combine the records of multiple individuals.
Mercenaria stimpsoni is the most long-lived among modern bivalves living near the Japanese coast (Shirai et al. Reference Shirai, Kubota, Murakami-Sugihara, Seike, Hakozaki and Tanabe2018), and its shell growth pattern and the paleoenvironmental implications of the pattern have been documented previously (Tanabe et al. Reference Tanabe, Mimura, Miyaji, Shirai, Kubota, Murakami-Sugihara and Schone2017; Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Hori and Tanabe2017, Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a; Shirai et al. Reference Shirai, Kubota, Murakami-Sugihara, Seike, Hakozaki and Tanabe2018). This species inhabits fine sandy substrata in the shallow coastal zone (water depth 5–30 m) along mid- to high-latitude coasts of the northwest Pacific, the Sea of Japan, and the Sea of Okhotsk (Habe Reference Habe1977). It is an infaunal filter feeder that consumes phytoplankton (predominantly diatoms) and suspended organic matter (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Hori and Tanabe2017; Seike et al. Reference Seike, Shirai and Kubota2017). At ontogenetically younger stages (<15 years old), the shells grow from early spring to late summer at a relatively high rate (∼10 mm/yr), but shell growth ceases or is substantially reduced during winter, when the water temperature is below ∼10°C (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Hori and Tanabe2017). At ontogenetically older stages (>15 years), shell growth occurs only in summer and the growth rate is very low (0.05–0.1 mm/yr). Growth cessation lines are visible in shell cross sections, and the calendar year of past growth increments of a live-caught clam can be obtained by counting the annual growth lines backward from the most recent (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a; Shirai et al. Reference Shirai, Kubota, Murakami-Sugihara, Seike, Hakozaki and Tanabe2018).
Many dead M. stimpsoni shells can be found on the seafloor of Funakoshi Bay. While a modern specimen provides a record that extends back to when the specimen first developed a shell, by combining, through crossdating (e.g., Black et al. Reference Black, Griffin, van der Sleen, Wanamaker, Speer, Frank, Stahle, Pederson, Copenheaver and Trouet2016), the annual growth increment records of modern specimens with those of specimens that lived during an earlier period, the paleoenvironmental record can be extended further back in time to produce a master chronology. However, to obtain a continuous record with annual resolution, we need to determine the dates of death of dead shells very precisely, with a precision of one year. However, crossdating of dead shells is more complicated than crossdating of live-caught specimens because the record of a dead shell, especially if it is short, may match several calendar year intervals in the master chronology. Conventional radiocarbon dating of marine samples has a large age determination error of more than ±50 years, which stems from the analytical precision and uncertainties of the seawater 14C calibration curve (e.g., Marine20, Heaton et al. Reference Heaton, Köhler, Butzin, Bard, Reimer, Austin, Bronk-Ramsey, Grootes, Hughen, Kromer, Reimer, Adkins, Burke, Cook, Olsen and Skinner2020) and the marine 14C reservoir age (Alves et al. Reference Alves, Macario, Ascough and Bronk-Ramsey2018). One way to overcome this problem is to use 14C produced by atomic bomb testing (Hua et al. Reference Hua, Barbetti and Rakowski2013). Intense atmospheric testing of thermonuclear weapons conducted in the 1950s and 1960s artificially produced 14C through reactions of high-energy neutrons with atmospheric nitrogen (bomb-14C). The bomb-14C entered the Earth surface system and has already been widely used as a tracer for studying biogeochemical cycles and to estimate the longevity of both terrestrial and marine organisms (Kalish Reference Kalish1993; Campana et al. Reference Campana, Natanson and Myklevoll2002; Hamady et al. Reference Hamady, Natanson, Skomal and Thorrold2014; Nielsen et al. Reference Nielsen, Hedeholm, Heinemeier, Bushnell, Christiansen, Olsen, Bronk Ramsey, Brill, Simon and Steffensen2016).
Although mixing occurs rapidly in the atmosphere, in seawater mixing occurs more slowly; as a result, bomb-14C is heterogeneously distributed in the surface of the ocean (Mahadevan Reference Mahadevan2001; Druffel Reference Druffel2002; Grottoli and Eakin Reference Grottoli and Eakin2007; Scourse et al. Reference Scourse, Wanamaker, Weidman, Heinemeier, Reimer, Butler, Witbaard and Richardson2012; Toggweiler et al. Reference Toggweiler, Druffel, Key and Galbraith2019). Therefore, to use the bomb-14C record as an age-determination tool, a continuous regional bomb-14C record must first be established. Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a) established a bomb-14C record for Funakoshi Bay by crossdating the 6 live-caught M. stimpsoni individuals mentioned above (this study improved the curve by adding 4 new data points; see Online Supplementary Material).
In the present study, we used crossdating and the bomb-14C record to determine the precise (annually resolved) ages of dead shells of M. stimpsoni collected from the seafloor of Funakoshi Bay. We then compared our analysis results with the timing and amplitude of past tsunamis to determine how they might have affected the mortality of this species in the bay. We also measured the 14C content of an articulated M. stimpsoni shell found in a marine sediment core obtained from tsunami deposits in Funakoshi Bay in 2014. The goal of this study is to assess how past tsunamis, especially one occurred at 11 March 2011, affected the mortality of M. stimpsoni in Funakoshi Bay.
METHODS
Funakoshi Bay is located on a ria coast, a part of the Sanriku coast of northeastern Japan (Figure 1). The coastal plain along this section of coast is narrow, and the bay, which faces the open ocean, is directly affected by ocean wave activity. The floor of the bay is covered by poorly sorted sand and inclines gradually toward the open ocean (Seike et al. Reference Seike, Shirai and Kogure2013). Otsuchi Bay is a rectangular bay, located immediately south of Funakoshi Bay, that measures 8 km from east to west and 2 km from north to south (Figure 1). Water depth increases gradually toward the bay mouth, where it reaches 70 m. Otsuchi Bay is fed by three main rivers (the Otsuchi, Kozuchi, and Unosumai Rivers). Each river discharges freshwater in the bay at a rate of 3–10 m3/s (Kubota et al. Reference Kubota, Shirai, Higuchi and Miyajima2018b).
Figure 1 (A) Location of study site. The star indicates the epicenter of the 2011 Tohoku-oki earthquake. (B) Bathymetric map of Funakoshi Bay and Otsuchi Bay (bathymetric contour interval, 10 m), modified from Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). Shells and seawater were sampled at location F-1 in Funakoshi Bay and at location O-3 in Otsuchi Bay.
In this study, we used 5 live M. stimpsoni specimens collected from the seafloor of Funakoshi Bay (site F-1, 20 m water depth; Figure 1) and 1 from Otsuchi Bay (site O-3, 5 m water depth) during a dive or by using a Smith–McIntyre mud sampler (see Online Supplementary Material) (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). These specimens were frozen after recovery and then transported to the laboratory for the removal of their soft tissues. In the laboratory, the shells were cleaned and dried at room temperature. We also collected both the right and left valves of dead shells (in rare cases articulate shells, too) of M. stimpsoni from the seafloor at site F-1 in Funakoshi Bay (Figure 1) during SCUBA dives. We selected 27 right valves of the dead shells for further analysis to avoid duplication of the analysis in the same individuals.
For the analysis we also used one articulated M. stimpsoni specimen (see Online Supplementary Material) that was removed from a sediment core (6 cm in diameter, 100 cm long) collected from the seafloor of Funakoshi Bay (F-1) in September 2014 (Seike et al. Reference Seike, Shirai and Kubota2017). The removed M. stimpsoni specimen was stored in a plastic bag until analysis. Sedimentary structures preserved in the core have already been reported in Seike et al. (Reference Seike, Shirai and Kubota2017). Briefly, the structures were examined by using a computed tomography (CT) scanner (LightSpeed Ultra16, GE Healthcare Japan Corp.) at the Center for Advanced Marine Core Research, Kochi University, Kochi, Japan. To observe both physical and biogenic sedimentary structures in the core, the CT scans were visualized by using OsiriX imaging software (version 4.1.2). After the core was scanned, it was sliced into 5-cm-long subsamples for analysis of the grain-size distribution with a laser granulometer (Mastersizer 2000, Malvern Instruments) at the Center for Advanced Marine Core Research.
The preparation of the live specimens for sclerochronological analysis was described by Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a), and the dead shells were prepared following the same method. First, we carefully removed materials adhering to the dead shell surfaces using a brush and then dried the shells at room temperature. From the 27 individuals, we selected 22 with relatively thick shells (i.e., with greater longevity), because short-lived individuals are not suitable for sclerochronological analysis. Then, each valve was wrapped in epoxy resin and sectioned from the umbo to the ventral margin along the maximum growth axis with a low-speed saw (Buehler Isomet). A cross-section was prepared and polished, and then images of the section were taken at 100× magnification with a KEYENCE digital microscope.
On the photographic image of each cross section, we counted the number of annual increments and measured their width by using ImageJ freeware (http://imagej.nih.gov/ij/). Growth in M. stimpsoni is similar to growth in trees in that growth increments vary in width and show strong ontogenetic trends (Tanabe et al. Reference Tanabe, Mimura, Miyaji, Shirai, Kubota, Murakami-Sugihara and Schone2017; Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Hori and Tanabe2017; Shirai et al. Reference Shirai, Kubota, Murakami-Sugihara, Seike, Hakozaki and Tanabe2018). We used the ARSTAN software package (https://www.ldeo.columbia.edu/tree-ring-laboratory/resources/software), following Butler et al. (Reference Butler, Richardson, Scourse, Witbaard, Schone, Fraser, Wanamaker, Bryant, Harris and Robertson2009a, Reference Butler, Scourse, Richardson, Wanamaker, Bryant and Bennell2009b), to produce a chronology by detrending and standardizing the time series data on annual growth increment widths. A negative exponential function was fitted to the time series of annual growth increment widths and then the residuals from the fitted function were calculated. We used the following equation to calculate the growth index (GI) for each year for each shell:
$${\rm{GI = }}{{{{\rm{m}}_{\rm{t}}}} \over {{{\rm{p}}_{\rm{t}}}}},$$
where m t is the measured annual increment width, and p t is the annual increment predicted from the fitted curve, at age t. Annual increment width records of modern shells has already been reported in Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a), but those of dead shell are reported in this study for the first time. Then we calculated the standardized shell growth index (SGI; Jones et al. Reference Jones, Arthur and Allard1989) from the GI:
$${\rm{SGI = }}{{({\rm{GI \,-\, }}{{\rm{x}}_{{\rm{GI}}}})} \over {{{\rm{s}}_{{\rm{GI}}}}}},$$
where x is the average and σ is the standard deviation of all GI values of the time series. The SGI is a dimensionless measure of shell growth that can be used for direct comparisons of shell growth between different specimens and different ontogenetic stages. According to Black et al. (Reference Black, Griffin, van der Sleen, Wanamaker, Speer, Frank, Stahle, Pederson, Copenheaver and Trouet2016), we visually crossdated both the live-caught and dead shells to produce a master chronology for the study area. We also calculated the expressed population signal (EPS) to evaluate the strength of the correlations among the individual time series and between those time series and the master chronology (Wigley et al. Reference Wigley, Briffa and Jones1984). Window length was set to 10 years in this exercise.
In this study, we used the time series data of annual growth increment widths for the shells of the 6 live-caught clams reported by Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a), together with data from 15 dead shells (among the 27 14C-dated dead shells), reported here for the first time. In 22 dead shells that were sclerochronologicaly analyzed 7 showed little annual variation and was not able to obtain dates, thus we did not include them in the master chronology. A cross section of the articulated M. stimpsoni specimen was not made because the shell was broken during coring (see Online Supplementary Material).
To obtain the most recent record from each shell, we traced the surface of the last-precipitated portion of the shell (last increment; see Online Supplementary Material) with a grinder to remove surface contamination and then collected calcium carbonate powder from the fresh surface. We also sampled the articulated M. stimpsoni from the sediment core in this manner.
We first photographed each cross section. Then we used a high-precision micromilling system (Geomill326, Izumo Web, Japan) and a triangular tungsten carbide drill bit (Shofu) and drilled into the outer shell layer to obtain samples of the annual growth layers for 14C analysis (e.g., Kubota et al. Reference Kubota, Yokoyama, Ishikawa and Suzuki2015a, Reference Kubota, Yokoyama, Kawakubo, Seki, Sakai, Ajithprasad, Maemoku, Osada and Bhattacharya2015b, Reference Kubota, Shirai, Murakami-Sugihara, Seike, Hori and Tanabe2017; Sakamoto et al. Reference Sakamoto, Komatsu, Yoneda, Ishimura, Higuchi, Shirai, Kamimura, Watanabe and Kawabata2017). By centering the drilling path on a relatively wide annual growth increment (length ∼10 mm, width 0.8 mm, depth 1.4 mm), 10–15 mg of calcium carbonate powder was obtained (see Online Supplementary Material). After drilling, we examined the drilled cross section to estimate the period of time-averaging and the mean number of years represented by each powder sample (see Online Supplementary Material).
Most of the radiocarbon analysis results for the live-caught shells (20 of 24 14C data points) have already been reported by Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a), but all radiocarbon data of dead shells are reported here for the first time. Five calcium carbonate powder samples were submitted to Paleo Labo Co. Ltd., Gifu, Japan, for routine 14C analysis with a compact accelerator mass spectrometer (AMS; NEC, USA). Other calcium carbonate powder samples were reacted with phosphoric acid, and the carbon dioxide produced was converted to graphite by a Fe catalyst at 620°C for 6–12 hr. The target graphite samples were measured with a Tandetron AMS (High Voltage Engineering Europa, the Netherlands) installed at the Institute for Space–Earth Environmental Research, Nagoya University.
The 14C measurements are expressed as the fraction of modern 14C, F14C, calculated with the following equation:
$${{\rm{F}}^{{\rm{14}}}}{\rm{C = }}{{{{\rm{A}}_{{\rm{SN}}}}} \over {{{\rm{A}}_{{\rm{ON}}}}}},$$
where ASN and AON are the 14C/12C ratios of the sample and of the NIST oxalic acid standard (HOxII), respectively, normalized to δ13CPDB = −25‰. The error of the F14C analysis by Paleo Labo was better than 0.0026 (1σ; see Online Supplementary Material). The error of the F14C analysis at Nagoya University was better than 0.0040 (1σ), except for two samples (0.0070 and 0.0068) with low beam intensities (see Online Supplementary Material).
The time averaging of the samples drilled from the live-caught specimens was 1–7 years, but in half of the samples, high-resolution sampling of <2 years was achieved (see Online Supplementary Material). We previously confirmed that 14C of the last increment of live-caught individuals represents that of dissolved inorganic carbon in the seawater (for details, see Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). For samples that died in the pre-bomb era, conventional 14C ages were converted to calendar ages before 1950 CE by using the Marine20 calibration curve (Heaton et al. Reference Heaton, Köhler, Butzin, Bard, Reimer, Austin, Bronk-Ramsey, Grootes, Hughen, Kromer, Reimer, Adkins, Burke, Cook, Olsen and Skinner2020) and the local marine 14C reservoir age of −49 ± 20 14C yr, which was calculated by using 7 14C measurements of the pre-bomb era portion of live-caught individuals (Alves et al. Reference Alves, Macario, Ascough and Bronk-Ramsey2018) (see Online Supplementary Material).
RESULTS
The present study added 4 new 14C data points to the bomb-14C record for Funakoshi Bay established by Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). The expanded record improves the time resolution of the period from 1953 to 1963. We also merged radiocarbon data (6 data points) from the live-caught M. stimpsoni shell from Otsuchi Bay (specimen 120901OTW_alive), which is immediately south of Funakoshi Bay (Figure 1), with the bomb-14C record for Funakoshi Bay, because there is no discernible difference in seawater and shell F14C values between the two bays (for more details, see Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). One likely reason of similar 14C content irrespective of river water input is that freshwater run away at the very surface (0–3 m) of the Otsuchi Bay. (e.g., Tanaka et al. Reference Tanaka, Komatsu, Itoh, Yanagimoto, Ishizu, Hasumi, Sakamoto, Urakawa and Michida2017). In the refined bomb-14C record, the last appearance of pre-bomb 14C is in 1955 (in the previous record, it is 1952).
In the refined bomb-14C record F14C value is approximately constant at about 0.9333 until 1956 (Figure 2), and then it increases rapidly until 1974 to a peak of 1.1102. After this peak, F14C values gradually decrease, to 1.0238 ± 0.0027 in 2012 and to 1.0239 ± 0.0024 in 2016. These values are in good agreement with F14C values of dissolved inorganic carbon of the in-situ seawater (1.0263 ± 0.0066, N = 10), indicating that the shells directly record seawater 14C (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). Furthermore, these values are almost identical to the average F14C value of atmospheric CO2 (1.0256 ± 0.0078, N = 59 for 2012–2016, based on monthly observations at Schauinsland, Germany, by Heidelberg University: Hammer and Levin Reference Hammer and Levin2017). The peak value of 1.1102 corresponds to 70% of the peak value of surface water in the North Pacific subtropical gyre (the highest seawater value) and to 11% of the peak atmospheric value (e.g., Konishi et al. Reference Konishi, Tanaka and Sakanoue1981; Fallon and Guilderson Reference Fallon and Guilderson2008; Glynn et al. Reference Glynn, Druffel, Griffin, Dunbar, Osborne and Sanchez-Cabeza2013; Andrews et al. Reference Andrews, Asami, Iryu, Kobayashi and Camacho2016; Hirabayashi et al. Reference Hirabayashi, Yokoyama, Suzuki, Miyairi and Aze2017). Given that the estimation error of F14C is about 0.0030, the bomb-14C peak is strong enough to be used for age determination of the dead shells.
Figure 2 (A) Bomb-14C record of the study area that was created by using 6 live-caught individuals (black line with circles) (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). The F14C values of the last increment (yellow circles) and inner parts (red squares) of the shells of clams that were likely killed by the March 2011 tsunami are also shown. The horizontal error bars of the red squares represent the period of time averaging, not the dating uncertainty. (B) From left to right: F14C values of the last increments of shells of clams that were likely killed by the March 2011 tsunami (yellow circles), a buried articulate dead shell found within the tsunami deposits (purple diamond), and live-caught individuals (black circles), together with the dates on which they were collected.
We found that the correlation between an average of standardized shell growth indexes (SGI) of the 6 live-caught individuals and the SGIs of 10 dead shells was statistically significant in all combinations (r = 0.57–0.92, p < 0.01; see Online Supplementary Material). We calculated these correlations for the records covering the years 1960–1985, rather than for the entire period of the sclerochronological record, because only during these years were statistically significant correlations found among the 6 live-caught individuals by Kubota et al. (Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). Among the 10 dead shells, the SGI of eight shells showed a statistically significant correlation with the average of the SGIs of the 6 live-caught individuals only if the last annual increment was produced in 2010; if the date of the last increment was shifted forward or backward by up to 5 years, no statistically significant correlation was found (see Online Supplementary Material). The SGI of 1 dead shell (specimen 110909FKW_dead_A02R) showed a statistically significant correlation with the master chronology if the last annual increment was produced in 2011 (r = 0.45, p = 0.02), but the correlation was stronger if the increment was precipitated in 2010 (r = 0.66, p < 0.001) (see Online Supplementary Material). The SGI of the 10th dead shell (specimen 160608FKW_dead_A14R) showed a statistically significant correlation with the average of the SGIs of the 6 live-caught individuals if the date of the last increment was 2015. The master chronology in this study area extended back to 1890, and the expressed population signal (EPS) calculated by the ARSTAN software for the 6 live-caught individuals and the 9 dead shells that most likely died in 2010 was higher than 0.85 during 1960–1985, when the SGI variability was particularly large; this EPS value is generally accepted to indicate an adequate level of correlated variation among populations. This EPS result indicates the existence of shared patterns of variation among individual clams, at least during this time interval (Figure 3).
Figure 3 (A, B) Variations in the annual growth increment widths of the 6 live-caught individuals and the 9 shells of clams that were likely killed by the March 2011 tsunami. (C) Standardized growth indices (SGIs) of the 15 live-caught and dead shells. (D, E) Expressed population signal (EPS) (D) and the number of M. stimpsoni shells contributing to the reconstruction (sample depth) (E). The pink dashed line represents EPS value of 0.85, which is the EPS value generally accepted to indicate that a statistically significant level of co-variation among populations (see main text). EPS is case sample numbers are less than 5 is not shown here. Note that patterns of SGI variation agree well among individual shells, especially during the years 1960–1985.
DISCUSSION
Timing of Death of M. stimpsoni
The radiocarbon dating results (see Online Supplementary Material) showed that, among the 27 dead shells of M. stimpsoni dated in this study, 7 of the clams died in the pre-bomb era and the others died in the post-bomb era. In this study, we focused on the 20 individuals that died in the post-bomb era. Because the dating error for pre-bomb era specimens is as large as 50 years, it is difficult to establish a causal relationship between the time of death and the timing of tsunamis or other environmental events. The 14C value of the last annual increment of these 20 individuals suggests that 10 of them (5 collected in September 2011 and 5 in June 2016) died around 2010. The F14C values of the last increments of these 10 dead shells (1.0157–1.0411) are consistent with those of individuals collected alive in 2010, 2012, and 2016 (1.0238–1.0344) (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a). On the other hand, the F14C values of the ontogenetically younger portions of these 10 dead shells were 1.0465–1.1184 (that is, the portion with mean growth years centered on 1965–1981; note that the time-averaging period of each sample was large, up to 16 years, because the slow-growing part of each shell was sampled). These values are in excellent agreement with the expected values based on the bomb-14C record for Funakoshi Bay (Figure 2a).
The widths of the last annual increment can be used to constrain the timing of death with seasonal resolution. The last annual increments of 9 of the 10 individuals described above were as wide as the annual increments of the previous year. Therefore, the possibility that they died (and shell growth ceased) during the summer is low; that is, they died not in summer 2010, but later, after shell growth had ceased. Because the growth period of M. stimpsoni in Funakoshi Bay begins in June and continues until the following January, it is likely that these individuals precipitated their last shell increments in 2010, but died in early 2011. Thus, the March 2011 tsunami likely led to the deaths of these individuals. However, radiocarbon dating can only suggest that the specimens died around 2010 because, given the various uncertainties, it is quite difficult to obtain ages with the necessary precision of one year to identify the cause of death. These uncertainties arise from the analytical uncertainty of the radiocarbon measurement, the slight differences in growth period (month) among individuals, the heterogeneity of seawater 14C, and the relatively large period of averaging of inner part of the shell required by the sampling technique.
However, by combining bomb-14C dating with a sclerochronological analysis, age determination with a one-year precision is possible (we selected only relatively long-lived individuals for sclerochronological analysis; thus, we have not been able to determine ages of all of the post-bomb specimens). To sum up the sclerochronological analysis, we found that among 14C-dated 10 individuals 9 died in 2010, but 1 (specimen 110909FKW_dead_A02R) died in 2015.
The F14C value of the last increment of 1 individual caught alive in September 2010 (100906FKW_alive) was 1.0344, which is in good agreement with the F14C values of 7 of 9 dead shells (1.0304–1.0411) (Figure 2). The F14C values of the other 2 dead shells, however, were only 1.0157 and 1.0163 (Figure 2). If only the F14C data are taken into account, it would seem that these 2 dead shells precipitated their last annual increment after 2010, because they were collected in 2016 from the seafloor and because there F14C values are closer to those of specimens caught alive in 2012 and 2016 (120901OTW_alive and 160608FKW_alive_01R, respectively). However, our sclerochronological analysis revealed that these 2 dead shells also precipitated their last annual increment in 2010 (r = 0.81–0.82, p < 0.0001; see Online Supplementary Material). The F14C values of the tenth individual inferred by radiocarbon dating alone to have died in 2010 (160608FKW_dead_14R) were 1.0195 for the last annual increment and 1.1035 for increments precipitated when it was ontogenetically younger. However, sclerochronological analysis of this specimen revealed that the last annual increment was precipitated in 2015 (r = 0.82, p < 0.0001) (see Online Supplementary Material). It is noteworthy that, different from the other 9 individuals inferred to have died in 2010, the last increment of this specimen was only half as wide as the increment of the previous year. Therefore, the shell growth in this individual was interrupted in summer 2015, when the individual died for an unknown reason (the summertime temperature in 2015 was not unusual). In summary, on the basis of 14C data alone, 10 individuals appeared to have died in 2010, but by combining 14C data with a sclerochronological analysis, it was possible to show that 1 of the 10 died not in 2010 but in 2015.
From these results, we inferred that the deaths of the 9 individuals (dead shells) that precipitated their last annual increments in 2010 were likely related to the March 2011 tsunami for the following reasons: (1) the F14C values of the last increments and of the inner parts of the dead shells coincided well with the bomb-14C record in the study area; (2) correlations between the average SGI of the live-caught individuals and the SGIs of the dead shells in all combinations were statistically significant; and (3) the width of the last increments showed that these animals died, not during the shell growth season, but later, after growth had ceased.
How Might the March 2011 Tsunami Have Caused the M. stimpsoni Deaths?
We showed that mass mortality in M. stimpsoni (9 of 20 individuals that died in the post-bomb era) was likely related to the March 2011 tsunami, but other possible reasons for this mass mortality need to be carefully addressed. In particular, during winter 2010 to spring 2011, water temperature may have become unsuitable or predation by other animals may have increased. With regard to the former, the mean bottom water temperature in March 2011 was 7.05°C, 0.97°C higher than the 30-year climatological mean; therefore, unsuitably high water temperatures probably did not cause death in M. stimpsoni, because this clam species can survive and grow (calcify) in water temperatures of up to ∼20°C in summer. This species is considered to have a wide temperature tolerance because it is distributed over a wide latitudinal range in the northwest Pacific, from temperate to subpolar regions (e.g., off South Korea, Khim et al. Reference Khim, Je, Han, Woo and Park1998; off Hokkaido, northern Japan, Tanabe et al. Reference Tanabe, Mimura, Miyaji, Shirai, Kubota, Murakami-Sugihara and Schone2017). This wide temperature tolerance suggests that it is unlikely that unsuitable temperatures were a major cause of death of this clam. With regard to the latter, it is also unlikely that predation by other animals caused mass mortality in this clam for three reasons: (1) M. stimpsoni lives beneath the seafloor and is thus inaccessible to many predators; (2) the thick shells of adult individuals protect them from predation; and (3) the shells did not show any damage, such as holes drilled by carnivorous gastropods, or other signs of predation (Nakaoka Reference Nakaoka2000; Chiba and Sato Reference Chiba and Sato2013).
The distribution of tsunami deposits in Funakoshi Bay suggests that the seafloor was first greatly eroded by sub-bottom flows caused by the tsunami and subsequently covered by laminated tsunami deposits (Seike et al. Reference Seike, Shirai and Kubota2017, Reference Seike, Sassa, Shirai and Kubota2018). Clams that became buried beneath these tsunami deposits might have suffocated because they were unable to escape from deep burial. This possibility is supported by the finding of an articulated dead shell within the tsunami deposits; furthermore, the F14C value of the last annual increment of this shell (1.0392) was close to those of specimens caught live during 2010–2016 and also to those of the clams that died in March 2011. However, sclerochronological analysis of this shell was not performed because the shell became broken during the coring (Figure 2). It is also possible that sediment liquefaction caused by ground shaking during the earthquake caused M. stimpsoni individuals to become exposed above the seafloor, because density of this animal is lower than that of the ambient substrate (Seike et al. Reference Seike, Sassa, Shirai and Kubota2019). Such exposure might lead to the death of individuals that were not able to re-enter the sediment (e.g., by predation by octopus). Although it is clear that the mass mortality of M. stimpsoni was related to March 2011 earthquake and tsunami, the specific mechanism of death is difficult to determine. Because we collected dead shells only from the seafloor surface, we do not know whether many dead individuals might remain buried in the tsunami deposits, although wave action associated with, for example, an atmospheric low pressure system might bring some once-buried individuals to the seafloor.
Relationship between M. stimpsoni Deaths and Past Tsunamis
Although the deaths of at least 9 of the 27 studied individuals collected as dead shells were related to the March 2011 earthquake and tsunami, the other deaths did not coincide with the occurrence of a tsunami. Among those clams that died during the post-bomb era, 14C dating and sclerochronological analysis revealed that 2 individuals died in 1966 and 4 others died in 1968, 1971, 1986, and 2015 (Figure 4). Because neither water temperature (high or low) nor the shell growth period (longer or shorter) were unusual in these years, no environmental factor seems to have directly influenced their deaths. Furthermore, it is noteworthy that we found no evidence that the tsunami generated by the 1960 Chilean earthquake that struck northeast Japan in 1960 caused mass mortality of M. stimpsoni (Figure 4). One possible reason is that the amplitude of the 1960 tsunami (maximum run-up height along the Japanese coast was ∼6 m) was not large enough to disturb the seafloor environment and damage the benthic community. It would be worthwhile to test this hypothesis by collecting and dating additional dead shells.
Figure 4 (A) Bomb-14C record of the study area as in Figure 2 (black line with circles) (Kubota et al. Reference Kubota, Shirai, Murakami-Sugihara, Seike, Tanabe, Minami and Nakamura2018a) and the F14C values of the last increment of post-bomb era dead shells collected from the seafloor of Funakoshi Bay (red squares). Black arrows show the dates of major tsunamis that have struck northeastern Japan during the post-bomb era. (B) Block plot of the 1σ (68%, thick bars) and 2σ (95%, thin bars) calibrated age ranges for pre-bomb era dead shells collected from Funakoshi Bay, as determined by conventional radiocarbon dating. Black arrows at the top of the panel indicate the dates of major tsunamis that struck northeastern Japan during the pre-bomb era. It is difficult to associate any tsunami with the deaths of M. stimpsoni that died during the pre-bomb era because of the relatively large dating errors.
Huge tsunamis strike coastal northeastern Japan at intervals of 50–100 years, so it is possible that past tsunamis similar in scale to the March 2011 tsunami might have caused mass mortality of M. stimpsoni. One huge tsunami occurred in 1933 (Showa Sanriku earthquake: run-up height, ∼29 m) and another in 1896 (Meiji Sanriku earthquake: run-up height, ∼38 m). However, it is not possible to link a tsunami occurring during the pre-bomb era with the time of death of M. stimpsoni individuals by using only conventional 14C dating. The time of death estimated by conventional 14C dating of the 7 individuals that died during the pre-bomb era overlap with the occurrence times of these two tsunamis (Figure 4), but to confirm this association, it will be necessary to extend the master chronology further back in time.
The oldest clam among the live-caught individuals was 92 years old (Shirai et al. Reference Shirai, Kubota, Murakami-Sugihara, Seike, Hakozaki and Tanabe2018), but one of the dead shells was from an individual that had lived for 135 years (110909FKW_dead_B01R). Therefore, there is a chance that additional long-lived individuals will be found by future field surveys. Intriguingly, the longer-lived individual (and many others) must have survived two huge tsunamis, the Showa Sanriku earthquake tsunami in 1933 and the Meiji Sanriku earthquake tsunami in 1896, only to be killed by the March 2011 tsunami. Without the huge environmental disturbance caused by the tsunami, this animal might have lived even longer. Our findings imply that tsunamis act as a constraint on the longevity of M. stimpsoni clams living in this region. It would be worthwhile to test this idea by comparing the longevity of M. stimpsoni living in this region with that of this species living in other regions that rarely experience tsunamis.
CONCLUSIONS
By combining 14C and sclerochronological analyses, we showed that many individuals of the long-lived bivalve M. stimpsoni in Funakoshi Bay died during the huge tsunami that took place in March 2011. Further extension of crossdated annual growth increment records should make it possible to identify past mass mortality events related to tsunamis. In particular, the association of M. stimpsoni deaths with the tsunamis that occurred in 1933 and 1896 should be investigated by the method used here for the March 2011 tsunami. The 1896 tsunami occurred in June, which is during the M. stimpsoni shell growth season; thus, evidence for the tsunami may be recorded in the shell by trace element variations, as Murakami-Sugihara et al. (Reference Murakami-Sugihara, Shirai, Hori, Amano, Fukuda, Obata, Tanaka, Mizukawa, Sano and Takada2019) demonstrated in mussel shells. Trace elements in the shell of an individual that experienced the 1896 tsunami as a juvenile, when its annual shell growth rate was large, might serve as a distinct time marker and chronological constraint.
This dating method based on bomb-14C and sclerochronological analyses of the shells of a long-lived bivalve presented in this study can be applied to the shells of other mollusks that inhabit the Pacific coastal waters of Japan or other oceanic regions affected by tsunamis. However, application of this method to bivalves living in regions where the bomb-14C peak is dampened (e.g., upwelling and high-latitude ocean regions) would not be effective, nor is it applicable to bivalves that live at abyssal depths, where the amount of bomb-induced 14C is too small. Nevertheless, this method may prove effective for understanding the responses of shallow-water bivalve mollusks to environmental disturbances, especially in countries and remote regions where observations of past tsunamis are scarce. Further understanding of such responses may lead to better protection and sustainable use of fishery resources, especially commercially important shellfish.
ACKNOWLEDGMENTS
We thank T. Goto for cutting the M. stimpsoni shells at the Atmosphere and Ocean Research Institute, and A. Ikeda for the 14C analysis at the Institute for Space–Earth Environmental Research. Our gratitude is also extended to the ship crews of the International Coastal Research Center, the Atmosphere and Ocean Research Institute, and K. Fukuda (Fukuda Kaiyo Kikaku Ltd.) for help with field sampling. Part of the 14C analysis was performed by Paleo Labo Co., Ltd., under a Grant-in-Aid for Young Scientists to K. Kubota. This study was financially supported by Grants-in-Aid for Domestic Research from the Kurita Water and Environment Foundation (grant numbers 16B015 and 17K007) and the Joint Research Program of the Institute for Space–Earth Environmental Research to K. Kubota, Japan Society for the Promotion of Science Kakenhi grants (numbers JP13401521, JP16781047, and JP15647913/H05823) to K. Shirai, the cooperative research program of the Center for Advanced Marine Core Research, Kochi University (number 14B024) to K. Seike, and the research program “Tohoku Ecosystem-Associated Marine Sciences” of the Ministry of Education, Culture, Sports, Science and Technology. All data used are listed in the tables. Finally, we are grateful to the two anonymous reviewers, whose comments substantially improved this manuscript.
Supplementary material
To view supplementary material for this article, please visit https://doi.org/10.1017/RDC.2021.98
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