Variation in brachiopod microstructure and isotope geochemistry under low-pH–ocean acidification conditions
- 1Università degli Studi di Milano, Dipartimento di Scienze della Terra “A. Desio”, Milan, 20133, Italy
- 2GEOMAR Helmholtz-Zentrum für Ozeanforschung Kiel, 24148 Kiel, Germany
- 3Department of Earth Sciences, Brock University, St. Catharines, Ontario L2S 3A1, Canada
- 4Alfred-Wegener-Institut Helmholtz-Zentrum für Polar- und Meeresforschung, 27515 Bremerhaven, Germany
- 5ThermoFisher Scientific, Hanna-Kunath-Str. 11, 28199 Bremen, Germany
Correspondence: Facheng Ye (firstname.lastname@example.org)
In the last few decades and in the near future CO2-induced ocean acidification is potentially a big threat to marine calcite-shelled animals (e.g. brachiopods, bivalves, corals and gastropods). Despite the great number of studies focusing on the effects of acidification on shell growth, metabolism, shell dissolution and shell repair, the consequences for biomineral formation remain poorly understood. Only a few studies have addressed the impact of ocean acidification on shell microstructure and geochemistry. In this study, a detailed microstructure and stable isotope geochemistry investigation was performed on nine adult brachiopod specimens of Magellania venosa (Dixon, 1789). These were grown in the natural environment as well as in controlled culturing experiments under different pH conditions (ranging from 7.35 to 8.15±0.05) over different time intervals (214 to 335 days). Details of shell microstructural features, such as thickness of the primary layer, density and size of endopunctae and morphology of the basic structural unit of the secondary layer were analysed using scanning electron microscopy. Stable isotope compositions (δ13C and δ18O) were tested from the secondary shell layer along shell ontogenetic increments in both dorsal and ventral valves. Based on our comprehensive dataset, we observed that, under low-pH conditions, M. venosa produced a more organic-rich shell with higher density of and larger endopunctae, and smaller secondary layer fibres. Also, increasingly negative δ13C and δ18O values are recorded by the shell produced during culturing and are related to the CO2 source in the culture set-up. Both the microstructural changes and the stable isotope results are similar to observations on brachiopods from the fossil record and strongly support the value of brachiopods as robust archives of proxies for studying ocean acidification events in the geologic past.
Since the industrial revolution the surface ocean pH has dropped by 0.1 units and is predicted to drop another 0.3–0.5 units by 2100 (Caldeira and Wickett, 2005; Orr et al., 2005; IPCC, 2013). This is due to the increasing amount of atmospheric carbon dioxide (CO2) absorbed by the ocean that extensively affects seawater carbonate chemistry (e.g. Caldeira and Wickett, 2003, 2005; Orr et al., 2005; Feely et al., 2004). Increased concentrations of anthropogenic CO2 are reflected in an elevated concentration of hydrogen ions, which lowers the pH and the availability of carbonate ions. Effects on marine organisms are of great scientific interest for understanding the geological past and the consequences in the immediate future (e.g. Ries et al., 2009), since the decrease in calcium carbonate saturation potentially threatens marine organisms forming biogenic calcium carbonate (e.g. Orr et al., 2005; Guinott et al., 2006; McCulloch et al., 2012; Jantzen et al., 2013a, b). This applies to calcium carbonate shell-forming species, such as brachiopods and mollusks, because they are considered excellent archives documenting changes in environmental conditions affecting marine organisms (e.g. Kurihara, 2008; Comeau et al., 2009; Hahn et al., 2012, 2014; Watson et al., 2012; Cross et al., 2015, 2016, 2018; Crippa et al., 2016a; Milano et al., 2016; Garbelli et al., 2017; Jurikova et al., 2019).
Recently, several experiments were performed to investigate whether a change in seawater pH may affect growth rate, shell repair and oxygen consumption of calcifying organisms, and how they respond, in general, to ocean acidification (Supplement Table S1). However, despite the great number of studies, the consequences for biomineral formation remain not well understood, as most studies focused mainly on growth, metabolic rates, shell dissolution and shell repair (Table S1, and references therein). Only a few studies deal with the effect of acidification on microstructure (Beniash et al., 2010; Hahn et al., 2012; Stemmer et al., 2013; Fitzer et al., 2014a, b; Milano et al., 2016), and most of them focused on bivalves and show that neither microstructure nor shell hardness seem to be affected by seawater pH.
The few studies that examined brachiopods or brachiopod shells suggest that the latter suffered increased dissolution under lower seawater pH. In other studies, the organism either exhibited no changes or an increase in shell density (calculated as dry mass of the shell (g)/shell volume (cm3)), but otherwise no changes in shell morphology and trace chemistry (Table 1). Cross et al. (2018) found that punctae became narrower over the past 120 years, which partially explained the increase in shell density over this period. Overall, there appears to be little to no apparent effect on brachiopod morphology or chemistry with lower seawater pH (Cross et al., 2015, 2016, 2018).
* A subsample of 40 brachiopods (two to five specimens per decade over the last 120 years) were used for further shell analysis of shell density, punctal width, punctal density, shell dissolution, shell thickness and shell elemental composition.
Brachiopods possess a low-magnesium calcite shell, which should be more resistant compared to the more soluble forms of CaCO3 such as aragonite and high-Mg calcite (Brand and Veizer, 1980; Morse et al., 2007). The shell microstructure of Rhynchonelliformean brachiopods has been used as a powerful tool to understand the biomineral's response to modern global ocean acidification and similar events in the geologic past (Payne and Clapham, 2012; Cross et al., 2015, 2016; Garbelli et al., 2017). A comprehensive study focusing on fossil brachiopods during the end-Permian mass extinction showed that brachiopods produce shells with increased organic matter content during ocean acidification events (Garbelli et al., 2017).
Here, we describe the microstructure and carbon and oxygen isotopic composition of brachiopod shells belonging to the cold–temperate water species Magellania venosa (Dixon, 1789) grown in natural environments as well as under pH-controlled culturing conditions. M. venosa represents the largest recent brachiopod species, is often locally abundant (e.g. in Chile; Försterra et al., 2008), and has the highest growth rate recorded for recent brachiopods (Baumgarten et al., 2014). Its low-magnesium calcite shell consists of a microgranular primary layer and a fibrous secondary layer (Smirnova et al., 1991; Baumgarten et al., 2014; Casella et al., 2018; Romanin et al., 2018) crossed by perforations – endopunctae.
Since little is known about the microstructural and geochemical responses of brachiopods to increased ocean acidification, the main goal of this study is to document any changes in this highly important archival marine organism. We will describe whether and how shell microstructural features such as the primary layer thickness, density of endopunctae and fibre morphology, together with their stable carbon (δ13C) and oxygen (δ18O) isotope compositions, respond to low seawater pH conditions.
2.1 Brachiopod samples and culturing set-up
A full description of the brachiopod sampling and culturing procedure is provided in Jurikova et al. (2019), but we provide an abbreviated version and reiterate the key points. Nine adult individuals of M. venosa (Dixon, 1789) were chosen for microstructure investigation and evaluation of their δ13C and δ18O values. All specimens were collected by scientific SCUBA divers alive from 20 m water depth of Comau Fjord (Chile) at different localities (Fig. 1). Specimens no. 158 and no. 223 did not experience any treatment after collection from Comau Fjord. The other specimens, no. 43, no. 63, no. 8004, no. 8005, no. 9004, no. 9005 and no. 9006, were cultured under different pH conditions at either AWI in Bremerhaven or GEOMAR (at KIMOCC – Kiel Marine Organisms Culture Centre) in Kiel, Germany (Tables 2 and 3).
Note: D: depth (m), T: temperature (∘C), S: salinity (PSU – practical salinity units), pCO2 (µatm). 1 Cahuelmó 42∘15′23 S, 72∘26′42 W, Cross–Huinay 42∘23′28 S, 72∘27′27 W, Jetty (Huinay Dock) 42∘22′47 S, 72∘24′56 W, Lilliguapi 42∘9′43 S, 72∘35′55 W; sample nos. 8004, 8005, 9004, 9005, and 9006 were harvested from three sites in Comau Fjord (Cross-Huinay, Jetty, and Liliguapy), Chile. 2 Reference: Laudien et al. (2014) and Jantzen et al. (2017). 3 Culture experiments conducted at Alfred-Wegener-Institut Helmholtz-Zentrum für Polar- und Meeresforschung, Bremerhaven, Germany. 4 Culture experiments conducted at GEOMAR Helmholtz-Zentrum für Ozeanforschung Kiel, Germany (Jurikova et al., 2019). 5 CO2 concentration was changed during the experiment: to 2000 µatm from 4 August 2016 to 18 April 2017 and to 4000 µatm from 18 April to 5 July 2017.
In summary, individuals of M. venosa were collected alive in Chile and transported to GEOMAR, Germany, in plastic bags filled with seawater, and maintained under controlled conditions in a climate laboratory. The brachiopods were first acclimatized under control conditions for 5 weeks, and prior to the start of the experiment were labelled with a fluorescent dye – calcein (Sigma, CAS 1461–15–0; 50 mg L−1 for 3 h) (e.g. Baumgarten et al., 2014; Jurikova et al., 2019). As a culture medium we used artificial seawater, which was prepared by mixing a commercial salt with deionized water until the desired salinity and chemical composition were achieved (Atkinson and Bingman, 1998). An overview of the culturing set-up at both laboratories is available in Table 2. Specimens no. 43 and no. 63 were cultured at AWI at pH = 7.66 (pCO2 = 1390 µatm) and pH = 7.44 (pCO2 = 2610 µatm) from 29 August 2013 to 31 March 2014, respectively. Specimens nos. 8004, 8005, 9004, 9005 and 9006 were cultured concurrently at GEOMAR under control or low-pH conditions. Specimens no. 8004 and no. 8005 were maintained under pH settings of 8.0–8.15 from 4 August 2016 to 5 July 2017, conditions similar to those of their fjord habitat. In contrast, specimens nos. 9004, 9005 and 9006 were cultured under low-pH artificial seawater conditions. Low-pH conditions were achieved by bubbling of CO2 through the tanks at AWI, and by bubbling CO2-enriched air through the tanks at GEOMAR (Table 2). The acidification experiment at GEOMAR was performed in two phases; the first one from 4 August 2016 to 18 April 2017 during which the pCO2 was set to 2000 µatm (corresponding to a pH of 7.60), and the second one during which the pCO2 was set to 4000 µatm (corresponding to a pH of 7.35) from 18 April 2017 to 5 July 2017 (Table 3). In order to distinguish between the shell parts precipitated under the specific pH conditions as well as to allow exact comparison to shells of the control treatment, calcein marking was also carried out prior to the second low-pH experiment of 4000 µatm. Parts of the shell grown under specific pH conditions are indicated in Fig. 2. In addition to the calcein marking, newly grown shell parts may be distinguished from visible growth lines on the surface of the shell (Fig. 2). The total length (maximum distance from the blue line to the anterior margin) of the curved dorsal and ventral valves grown during 11 months of culturing (Fig. 2) varied from < 5 to 15.6 mm (Table 4).
2.2 Microstructural analysis
This study followed the sample preparation method shells suggested by Crippa et al. (2016b). In order to obtain more detailed data on microstructural changes, the samples were cut with a diamond blade along different axes and directions (Fig. 3a). Subsequently, the samples were immersed in 36-volume hydrogen peroxide (H2O2) for 24∕48 h to remove the organic tissue. The sectioned surfaces were manually smoothed with 1200 grit sandpaper, then quickly (3 s) cleaned with 5 % hydrochloric acid (HCl), immediately washed with water and air-dried. The time of acid etching was kept short so as not to affect the microstructure (Crippa et al., 2016b). Finally, the valve sections were gold-coated and analysed by a Cambridge S-360 scanning electron microscope with a lanthanum hexaboride (LaB6) source operating at an acceleration voltage of 20 kV (Dipartimento di Scienze della Terra “A. Desio”, Università di Milano).
The methods described by Ye et al. (2018a) were followed to investigate the basic microstructural units (fibres) in SEM images. We focused primarily on the anterior margin of the valves, the part that was produced during culturing (hereinafter referred to as during-culturing) under different pH conditions. Therefore, additional transverse sections along the growth lines were obtained in the most anterior part (black lines in Fig. 3b) by manually smoothing with 1200 grit sandpaper. Plane grinding was performed on the external surface of the shell (Fig. 3) to investigate the distribution of endopunctae.
The thickness of the primary layer was measured on the SEM images of specimens no. 8005 and no. 9006 (Fig. 4a) in different positions along the longitudinal growth axis (posterior, central and anterior regions). In the vicinity of the transition from natural growth to cultured growth, the region was further subdivided into four sub-zones.
To calculate and measure the density and diameter (max) of endopunctae, squares (800 µm × 800 µm) were located randomly over the smoothed external surface of the anterior shell (Fig. 4b). Four sub-zones (C2, A1, A2, A3) were defined according to their position along the posterior–anterior direction (Fig. 4), while distinguishing the part of the shell produced before-culturing and that produced during-culturing.
For morphometric analyses, fibres were manually outlined using polygonal lasso in Adobe Photoshop CS6, and size and shape parameters were measured with Image-Pro Plus 6.0 and ImageJ (for convexity). In particular, following Ye et al. (2018a, b) we measured/calculated the Feret diameter (max), area, roundness (4area/π× Feret diameter (max)2) and convexity (convex perimeter / perimeter). The width of an individual fibre roughly corresponds to its Max Feret diameter, whereas its height corresponds to the Min Feret diameter (see Fig. 6 in Ye et al., 2018a).
As individual fibres are irregular in shape in the most anterior section of brachiopods, the morphometric measurement method proposed by Ye et al. (2018a, b) is not always suitable. Thus, modifications had to be made to the Ye et al. (2018a, b) measurement method to make the comparative morphometric analysis of the fibres from the anterior part (Fig. 5a, b). First, all SEM images were oriented in the same direction with the base of the primary layer facing upwards. Then a uniformly sized zone (20 µm × 20 µm) was selected for additional measurements with the upper side of the square always placed at the boundary between the primary and secondary layers (Fig. 5c). Two new methods were developed and applied: for Method 1, the width of fibres crossed by two standard lines was measured, which were always located in the same position and at the same distance in all the selected zones (yellow and orange lines in Fig. 5, Method 1). For Method 2, we calculated the number of boundaries based on the number of fibres crossed by the two standard lines (Fig. 5, Method 2). Sub-zones were named according to the following nomenclature: the most anterior transection zone of the ventral valve was named Z1, the second most anterior transection zone of the ventral valve Z2, and so on; the most anterior transection zone of the dorsal valve was named Z4. The standard line facing the primary layer was named “1” and the second standard line “2” (example: “Z1-1” is the sample of the standard line facing the primary layer at the most anterior transect zone of the ventral valve).
2.3 Stable isotope analyses of shells
Cleaned shells of specimens nos. 8004, 8005, 9004, 9005 and 9006 were chosen for carbon and oxygen isotope analyses. For specimens no. 8005 and no. 9006, surface contaminants and the primary layer were first manually and then chemically removed by leaching with 10 % HCl, rinsed with distilled water and air-dried. As the primary layer is not secreted in equilibrium with ambient seawater (e.g. Carpenter and Lohmann, 1995; Brand et al., 2003, 2013), it is important to chemically remove it in order to avoid cross-contamination of results. Individual growth increments exclusively come from the secondary layer, and were separated from the shell in both dorsal and ventral valves using a WECHEER (WE 248) microdrill at low speed with a tungsten–carbide milling bit. Shell increment fragments, of similar width, were then powdered using an agate mortar and pestle. For carbon and oxygen isotope analyses about 250 µg of powdered calcite of each sample was analysed using an automated carbonate preparation device (GasBench II) connected to a Delta V Advantage (Thermo Fisher Scientific Inc.) isotopic ratio mass spectrometer at the Earth Sciences Department, University of Milan, Italy. The carbon and oxygen isotope compositions are expressed in the conventional delta notation calibrated to the Vienna Pee-Dee Belemnite (V-PDB) scale by the international standards IAEA 603 (International Atomic Energy Agency 603; δ18O: ‰, δ13C: ‰) and NBS 18 (δ18O: ‰, δ13C: ‰). Analytical reproducibility (1σ) for these analyses was better than ±0.04 ‰ for δ13C and ±0.1 ‰ for δ18O (Appendix A). Another set of shells, no. 8004, no. 9004 and no. 9005, were gently rinsed with ultra pure water (Milli-Q) and dried for a few days on a hotplate at 40 ∘C in a clean flow hood. Targeted parts of the shell were sampled for powder under binoculars using a precision drill (Proxxon) with a mounted dental tip. Stable isotope analyses of powders of these specimens were performed at GEOMAR, Kiel, on a Thermo Finnigan MAT 252 mass spectrometer coupled online to an automated Kiel carbonate preparation line. The external reproducibility (1σ) of in-house carbonate standards was better than ±0.1 ‰ and ±0.08 ‰ for δ13C and δ18O, respectively (Appendix A).
2.4 Stable isotope analyses of water samples
In addition to carbon and oxygen isotope analyses of shells, analyses were also carried out on seawater samples collected from the culturing tanks. Measurements of δ13CDIC and δ18O were performed using Thermo Scientific™ Delta Ray™ IRIS with URI Connect.
Isotope values (δ13C, δ18O) are reported as per mil (‰) deviations of the isotopic ratios (13C∕12C, 18O∕16O) calculated to the VPDB scale for δ13C and VSMOW scale for δ18O values. Analytical reproducibility (1σ) on three aliquots of each water sample was ≤0.03 ‰ for both δ13C and δ18O values (Appendix B).
3.1 Primary layer thickness
The thickness of the primary layer was measured at different positions along the shell from the posterior (umbonal) region to the before-culturing portion and finally to the anterior valve margin (Fig. 6). Generally, in the posterior part of M. venosa, the primary layer is missing or it has the lowest recorded thickness. Then, the primary layer progressively thickens toward the central and anterior parts. The thickest primary layer within the same valve is always located just before the beginning of the culture (before-culturing portion, Table 5). During-culturing the thickness of the primary layer decreases. A most distinct change was observed in specimen no. 9006 cultured at the lowest pH condition of 7.6, and of 7.35 followed by another progressive increase in both valves during-culturing. In contrast, the thickness of the primary layer of the control condition specimen (no. 8005) remained stable (dorsal valve) or slightly decreased (Fig. 6, ventral valve; Table 5).
3.2 Endopunctae density and size
On the externally ground surface of the anterior part, the total number and the diameter (max) of endopunctae in a squared area of 800 µm × 800 µm were measured in four before-culturing parts and of the during-culturing parts of the shell (Fig. 7). Generally, the density of endopunctae gradually increased along the selected transect from ca. 185 to ca. 305 mm−2 in the ventral valve and from ca. 220 to ca. 280 mm−2 in the dorsal valve (Table 6). The size of endopunctae increased along the selected transect in the ventral valve (from ca. 17 to 33 µm; Table 7), but it slightly decreases in the dorsal valve from ca. 36 µm to ca. 21 µm (Table 7). These density and size trends were observed in both specimens cultured under different pH conditions. However, it is noteworthy that in the most anterior part (during-culturing) of the ventral valve of no. 9006 (cultured at a pH of 7.35), the density of endopunctae sharply increases and their diameter reached recorded maximum values (Table 6).
3.3 Shell morphometrics
Ontogenetic variation in fibre morphometry is not obvious when all six adult specimens are considered (Table 8). However, clearer growth trends can be observed when considering the data from each single specimen separately, where t-tests on morphometric data from specimens no. 8005 and no. 9006 show that there are significant differences in Feret diameter (max) and roundness between the posterior and the middle part of the shell (Table 9). Overall, in specimens no. 8005 and no. 9006, fibres become wider from the posterior to mid-shell. In contrast, no. 63 shows an opposite trend along the posterior to mid-shell direction (Fig. 8). The fibre size and shape in the other specimens are rather constant.
Transverse sections obtained by smoothing of the anterior part of the shell allowed us to measure the width of 1392 fibres (Max Ferret diameter (max); see in Method 1) and select 388 sub-zones for fibre boundary calculation. In addition, they allowed us to focus on the parts that were produced under the different low-pH treatments (7.66, 7.60, 7.44, and 7.35, respectively).
In all six specimens, the width of fibres increases and the number of boundaries decreases along a transect from the more external sub-zone to the immediately inner sub-zone (e.g. Z1-1 to Z1-2; Z2-1 to Z2-2; and Z3-1 to Z3-2 in Fig. 9a, b, c, d). This means that within a 10 µm distance the sizes of fibres become larger from the exterior part to the interior part of the shell.
Results from specimen no. 9006 (pH: 7.60 and 7.35) were compared to those of control specimen no. 8005 (pH: 8.00 and 8.15). Specimen no. 9006 cultured under low-pH conditions (pH: 7.60 and 7.35) had narrower fibres and a higher number of fibre boundaries when compared to those of control specimen no. 8005 (Fig. 9a, c). It is worth noting that, in comparison between the two specimens, the fibres from Z1-2 and Z2-2 of no. 9006 are significantly smaller than those of no. 8005. However, there is no significant difference in the size of fibres from sub-zone Z3-2 between the two specimens (Table 10).
The results from specimens (no. 43 and no. 63) grown under low-pH conditions (pH: 7.66 and 7.44) for a short time interval of 214 days are difficult to interpret, as in this case there is no direct control experiment sample to compare with the cultured specimens (Fig. 9b, d). The specimens grown in the natural environment (no. 158 and no. 223) have different sizes and ages, and so different growth rates may affect the size of the fibres.
3.4 Stable isotopes
The carbon and oxygen isotope compositions were measured along the shell growth increments in the dorsal and ventral valves (Fig. 10). In the before-culturing part of the shell, δ13C values varied between −2.02 and +0.45 ‰ in control group specimens no. 8004 and no. 8005, whereas they varied between −9.24 and −0.53 ‰ in low-pH group specimens nos. 9004, 9005 and 9006. Similarly, in the before-culturing shell part, δ18O values varied between −2.39 and +0.21 ‰ in control group specimens no. 8004 and no. 8005, but varied between −4.92 ‰ and +0.05 ‰ in low-pH group specimens nos. 9004, 9005 and 9006.
In the during-culturing part, δ13C values varied between −6.80 and −1.34 ‰ in control group specimens no. 8004 and no. 8005, whereas they varied between −27.09 ‰ and −9.69 ‰ in low-pH group specimens nos. 9004, 9005 and 9006 (Fig. 10). Concomitantly, δ18O values varied between −6.80 ‰ and −1.34 ‰ in control group specimens no. 8004 and no. 8005, but varied between −6.97 ‰ and −5.29 ‰ in low-pH group specimens nos. 9004, 9005 and 9006 (Fig. 10).
A marked drop in δ13C and δ18O is recorded in the shell increments produced during-culturing, particularly so in the specimens grown under low-pH conditions of 7.60 and 7.35, where δ13C values decreased to −27.09 ‰ (Fig. 10).
4.1 Microstructure and organic component relationship
Before discussing whether and how acidification may affect the microstructure of the brachiopod shell, it is important to examine the relationship between the microstructure and the number of organic components within the shell. It has already been stated that, in fossil and recent brachiopods, different shell microstructures have different numbers of shell organic components (Garbelli et al., 2014; Garbelli, 2017; Casella et al., 2018; Ye et al., 2018a).
This holds true for most rhynchonelliformean brachiopods: the primary layer of M. venosa consists of acicular and granular calcite (Williams, 1968, 1973, 1997; MacKinnon and Williams, 1974; Williams and Cusack, 2007; Casella et al., 2018). Analyses of electron backscatter diffraction show that the primary layer is a thin nanocrystalline layer with higher micro-hardness and smaller-sized calcite crystallites compared to those of the secondary layer (Griesshaber et al., 2004). In addition, each spherical and small unit is coated by a mixture of organics and amorphous calcium carbonate (Cusack et al., 2010). This, per se, may suggest a higher amount of organic components associated with the primary layer in contrast to other shell layers (i.e. secondary or in some species tertiary layer), but it has never been proven.
In fossils, the primary layer is likely absent or, if present, diagenetically altered, and it will luminesce (Grossman et al., 1991), suggesting that higher amounts of organics may be present. However, this has also been ascribed to the incorporation of magnesium into the lattice (Popov et al., 2007; Cusack et al., 2008). A report of higher sulfur concentration in the primary layer of the brachiopod Terebratulina retusa may suggest the presence of a sulfur-rich organic component, but backscatter electron imaging revealed contradictory results (England et al., 2007). Cusack et al. (2008) showed that, in the same species, the sulfate concentration is higher in the primary layer than in the secondary layer.
Since there is no conclusive evidence for this observation, we cannot relate the increase in thickness of the primary layer to changes in organics within the shell. With respect to previous findings (Williams, 1966; Parkinson et al., 2005), our results show that the thickness of the primary layer of M. venosa is much less uniform and shows an increase with growth, which is more evident during-culturing under low-pH conditions. However, disturbances (stress condition with handling before and at the start of the culturing) may also cause an abrupt change in thickness.
Endopunctae, which during life are filled with mantle expansions, are widely distributed in the shell of M. venosa and show the superficial hexagonal close-packing pattern documented by Cowen (1966). The biological function of endopunctae is still controversial, with some suggesting that, generally in living organisms, they serve as support and protection structures (Williams, 1956, 1997), as sensors, or as storage and respiration features (Pérez-Huerta et al., 2009). With more endopunctae filled by mantle expansions, the amount of organic tissue would increase in the same volume of shell. The density of endopunctae has been related to temperature, as species living at higher temperatures have greater endopunctae density (Campbell, 1965; Foster, 1974; Peck et al., 1987; Ackerly et al., 1993). The present analyses support the concept that the increase in endopunctae density may be related in part to ontogeny and to low-pH conditions. This may be expected, as organisms living under low-pH conditions have to up-regulate their internal pH to be able to calcify, as demonstrated in M. venosa by Jurikova et al. (2019) and also observed in other calcifiers such as corals (McCulloch et al., 2012; Movilla et al., 2014). This would require a higher energy cost and a larger respiration/storage surface would satisfy this requirement.
In addition to the thickness of the primary layer and the density of the endopunctae, the size changes in the individual fibres within the fibrous secondary layer may also contribute to the variability in organic components. Most of the recent rhynchonelliformean brachiopods, and M. venosa in particular, possess a shell mainly made of a fibrous secondary layer (Williams, 1997; Parkinson et al., 2005; Williams and Cusack, 2007). Each fibre of this layer is secreted by the mantle and it is ensheathed by an organic membrane (e.g. Jope, 1965; Williams, 1968; MacKinnon, 1974; Williams and Cusack, 2007; Cusack et al., 2008; Casella et al., 2018). Thus, with a decrease in size but within the same shell volume the surface area increases and with it the number of organic components. Recently, the relationship between the size of fibres and shell organic components was discussed in detail (Garbelli, 2017; Garbelli et al., 2017; Ye et al., 2018a). The main conclusion is that the smaller the calcite fibres, the higher the organic component in the shell (cf. Fig. 11). Thus, smaller fibres and a greater endopunctae density may lead to higher organic content per shell volume (Fig. 11).
4.2 Low pH and brachiopod microstructure
Several studies tried to understand how marine carbonate-shelled animals respond to ocean acidification, such as brachiopods (McClintock et al., 2009; Cross et al., 2015, 2016, 2018; Jurikova et al., 2019), bivalves (e.g. Berge et al., 2006; McClintock et al., 2009; Beniash et al., 2010; Parker et al., 2010; Melzner et al., 2011; Talmage and Gobler, 2011; Amaral et al., 2012; Hiebenthal et al., 2013; Coleman et al., 2014; Gobler et al., 2014; Milano et al., 2016), cold-water scleractinian corals (e.g. Form and Riebesell, 2011; McCulloch et al., 2012; Jantzen et al., 2013b; Büscher et al., 2017) and sea urchins (Suckling et al., 2015) (Table S1). The results of these studies show that, in general, seawater acidification reduces the growth rate of marine calcifiers (Michaelidis et al., 2005; Shirayama and Thornton, 2005; Berge et al., 2006; Bibby et al., 2007; Beniash et al., 2010; Nienhuis et al., 2010; Thomsen and Melzner, 2010; Fernández-Reiriz et al., 2011; Melzner et al., 2011; Mingliang et al., 2011; Parker et al., 2011, 2012; Talmage and Gobler, 2011; Liu and He, 2012; Navarro et al., 2013; Milano et al., 2016).
For brachiopods, in the Liothyrella uva (Antarctic) and Calloria inconspicua (New Zealand), no ocean acidification effects on shell growth were detected by Cross et al. (2015, 2016, 2018), although the shells of the former species may rapidly dissolve in acidified waters (McClintock et al., 2009). However, C. inconspicua from the same locality in New Zealand (Paterson Inlet, Stewart Island) laid down a denser shell over the last 120 years, with nearby environmental conditions increasing by 0.6 ∘C from 1953 to 2016 and slightly increasing by 35.7 µatm in pCO2 from 1998 to 2016 (Cross et al., 2018). These changes are in line with global trends of ocean pH and temperature since the industrial revolution (Caldeira and Wickett, 2005; Orr et al., 2005; IPCC, 2013). The present experiment showed that growth of specimens was not affected by the low-pH conditions; instead, their growth was similar to that of specimens cultured under control conditions (no. 9006, ∼0.9 cm in the ventral valve, ∼0.8 cm in the dorsal valve; no. 8005, ∼0.5 cm in the ventral valve, ∼0.4 cm in the dorsal valve). Based on the von Bertalanffy growth function, Baumgarten et al. (2014) calculated an expected growth increment and rate, and we compared those parameters with the measured ones under control and low-pH conditions. The results in Fig. 12 demonstrate that the measured individual growth rates are within the range of the ones of naturally growing individuals.
A limiting factor is the small database, but in general, the present observations agree with studies that show no or little impact of acidification on the growth rates of marine calcifiers (cf. Marchant et al., 2010; Thomsen et al., 2010; Range et al., 2011, 2012; Talmage and Gobler, 2011; Dickinson et al., 2012; Fernández-Reiriz et al., 2012; Liu and He, 2012; Hiebenthal et al., 2013; Cross et al., 2015, 2016, 2018), or even an increase in respiration, shell growth or metabolic rates after having experienced low-pH conditions (Wood et al., 2008; Cummings et al., 2011; Parker et al., 2012). We note however that a combined effect of multiple stressors, such as low pH, lower dissolved oxygen and higher temperature or scarce food availability is more complex and potentially detrimental. For instance, Steckbauer et al. (2015) reported that hypoxia and increased pCO2 could significantly reduce the respiration rate of some marine invertebrates (Anthozoa, Gastropoda, Echinoidea and Crustacea). On the other hand, the highest growth rate in the bivalve Macoma balthica (Limecola balthica (Linnaeus, 1758)) was observed in seawater with low O2 and high pH (Jansson et al., 2015). Gobler et al. (2014) reported that juveniles of the bivalves Argopecten irradians (Lamarck, 1819) and Mercenaria mercenaria (Linnaeus, 1758) were not affected by hypoxia or acidification being applied individually, but the growth rate decreased when juveniles were exposed to both conditions simultaneously.
To explore the effects of acidification on brachiopod biomineralization, the microstructures of the specimens cultured for 214 days (no. 43, pH = 7.66±0.04; and no. 63, pH = 7.44±0.08) and the other population cultured for 335 days (no. 8005, pH = 8.0 to 8.15±0.05; and no. 9006, pH = 7.6 to 7.35±0.05) were investigated in detail. No conclusive consideration can be carried out on the specimens cultured for 214 days (no. 43 and no. 63), but in the other culturing experiments conducted for 335 days, the microstructure produced by the specimen cultured under low-pH conditions was different from that produced under control conditions: (1) the thickness of the primary layer increased with culturing (Fig. S1a–d); (2) the density and size of the endopunctae were higher (Fig. 1e–h); and (3) the fibres of the secondary layer were smaller. The punctal pattern detected here is different from that observed by Cross et al. (2018), who recorded no change in the punctal density of the ventral valve of C. inconspicua on specimens from the last 120 years. Also different is the trend in size of the endopunctae, which measured in the dorsal valve by Cross et al. (2018) seems to decrease. However, the slight environmental changes in the natural environment (references in Cross et al., 2018) are very different from those of our culturing experiments. Furthermore, the size of the endopunctae was measured from the dorsal valve only by Cross et al. (2018), whereas the increase in size we report was observed only from the ventral valve of M. venosa. A potential factor controlling this could be the duration of culturing under low-pH conditions. We note, however, that during the second phase of this acidification experiment (pH = 7.35), the seawater was strongly undersaturated with respect to calcite (Ωcal=0.6), suggesting that the observed structural changes could also be linked to the saturation state. Conversely, the duration of low-pH conditions as a controlling factor is also in line with the few data available in the literature on microstructural changes during acidification. Milano et al. (2016) reported no significant difference in the prismatic microstructure of the cockle Cerastoderma edule when cultured under low-pH conditions for about 2 months, except for dissolution of ontogenetically younger parts of the shell. Similarly, a study by Stemmer et al. (2013) on the clam Arctica islandica revealed that there was no effect on the shape and size of the crystals in the homogeneous microstructure after 3 months of culturing at low pH (Table S1). However, the experiments conducted by Fitzer et al. (2014a, b) for 6 months on the blue mussel Mytilus edulis showed that the animals exposed to low pH and high pCO2 tend to produce less organized, disorientated calcite crystals and an unordered layer structure.
Thus, in bivalves, and similar to our observations, the duration of culturing may be crucial in recording significant effects. The present results lend support to the microstructure variation observed in brachiopods during the end-Permian extinction event and concomitant ocean acidification (Garbelli et al., 2017). During this event, both Strophomenata and Rhynchonellata produced more organic-rich shells to cope with the long-term and protracted seawater acidification effects (Garbelli et al., 2017).
4.3 Stable isotope variation under low-pH conditions
Brachiopod shells are commonly used as archives for deep-time paleoenvironmental reconstructions as they potentially record the original geochemical composition of the seawater they lived in (Grossman et al., 1993; Banner and Kaufman, 1994; Mii and Grossman, 1994; Mii et al., 2001; Brand et al., 2003, 2011, 2016; Jurikova et al., 2019). Several studies suggest that carbon and oxygen isotope compositions of the secondary layer of brachiopod shells, especially slow-growing species – and particularly the innermost shell parts – tend to be close to equilibrium with the ambient seawater temperature (e.g. Popp et al., 1986; Carpenter and Lohmann, 1995; Parkinson et al., 2005; Brand et al., 2013, 2015, 2016; Takayanagi et al., 2013; Yamamoto et al., 2013). Recently, Bajnai et al. (2018) documented that brachiopods do not incorporate oxygen isotopes in thermodynamic equilibrium with ambient seawater, and appear to be subjected to taxon-specific growth-rate-induced kinetic effects. The documented isotopic offset appears to be relatively constant throughout the range of brachiopod shell production from cold to warm environments. Thus, the brachiopod oxygen isotope composition, when corrected for the seawater-18O contribution, records ambient water temperatures close to those observed for their ambient environment (Brand et al., 2013). Overall, the δ18O values of brachiopods remain a mainstay and robust proxies of paleoenvironmental temperature conditions.
In general, the measured δ13C (between −8.05 ‰ and +0.45 ‰) and δ18O (between −3.04 ‰ and +0.21 ‰) values of the secondary layer produced during growth in the natural environment (Fig. 10) are similar to previous results from the shells of M. venosa (Penman et al., 2013; Ullmann et al., 2017; Romanin et al., 2018). Furthermore, the present results show that there are no significant differences in δ13C and δ18O values between the dorsal and ventral valves (p-values in δ13C and δ18O of no. 8005 are 0.437 and 0.491, respectively, and p-values in δ13C and δ18O of no. 9006 are 0.862 and 0.910, respectively), which is in agreement with previous findings (e.g. Parkinson et al., 2005; Brand et al., 2015; Romanin et al., 2018).
In the naturally grown shell before-culturing, the δ13C and δ18O values are relatively stable along the ontogenetic direction (Table S2), except for the depleted values at approximately mid-shell length in both no. 8005 and no. 9006. In particular, in no. 9006, in this part of the shell values drop to about −6 ‰ for δ13C and −2 ‰ for δ18O values (Fig. 10). Since the samples were taken from the mid-shell layer and not from the shell interior, we can exclude the isotope negative shift being produced by shell material added during the during-culturing shell thickening. While this drop may be an artefact of both sampling and analytical uncertainties, a possibility also exists that it could be linked to shell repair processes. Brachiopods are well known to show a remarkable shell repair ability (Cross et al. 2015, 2016), and thus it cannot be ruled out that this shell part, although originally formed early in life under natural conditions, also contains a contribution from material precipitated in the culture seawater later in life, in particular under low-pH conditions. Also, negative isotope excursions of a similar magnitude were recorded in M. venosa specimens from the South America shelf by Ullmann et al. (2017) and Romanin et al. (2018). Ullmann et al. (2017) implied that these variable δ13C and δ18O values indicate isotope disequilibrium with ambient waters in Terebratellids. In contrast, Romanin et al. (2018), who also analysed specimens collected from Comau Fjord, attributed the negative isotope excursion to environmental perturbations, in particular, to changes in seawater productivity and temperature, and/or to anthropogenic activities. Negative shifts in both δ13C and δ18O values during ontogeny have also been observed in the brachiopod Terebratella dorsata, which co-occurs with M. venosa and which has been explained by the effect of resorption in corresponding muscle scar areas (Carpenter and Lohmann, 1995). Here, we follow the interpretation of Romanin et al. (2018) to explain the mid-shell excursion observed in our specimens.
The most prominent change in δ13C values was observed in the secondary layer produced during-culturing under low-pH conditions (δ13C VPDB: ‰), reflecting the composition of the δ13CDIC (δ13C VPDB: −24 ‰ for the low-pH/high-pCO2 conditions). The δ13C values were significantly depleted by more than 20 ‰ in the specimens cultured under low-pH/high-pCO2 conditions (pH 7.60 and pH 7.35; no. 9004, no. 9005 and no. 9006) (Fig. 10, Appendix A, Table S2), whereas the depletion was lower and only a few per mil (about 0.9 ‰–1.2 ‰) in the control specimens (pH 8.00 and 8.15; no. 8004 and no. 8005). This demonstrates that the δ13C values of M. venosa to a large extent reflect the composition of the CO2 source and thus present a valuable geochemical archive. Similar observations have also been reported for other calcifiers cultured under controlled experimental settings with pH mediated by CO2-bubbling. For a comparison, Hahn et al. (2014) reported a decreasing trend of about 10 ‰ in δ13C values in the blue mussel Mytilus edulis when exposed to seawater conditions of pH 8.03 (pCO2 612 µatm) and pH 7.21 (pCO2 4237 µatm). In corals, a species-specific δ13C response to high-pCO2 conditions was reported by Krief et al. (2010) of more negative 2.3 ‰ and 1.5 ‰ δ13C values in Porites sp. after 14 months of culturing under low-pH conditions (pH 7.49, pCO2 1908 µatm and 7.19 pCO2, 3976 µatm), whereas no significant difference was found in other coral species, such as Stylophora pistillata (Esper, 1797).
In our culturing experiments, oxygen isotope compositions of the shells record only a minor depletion during-culturing under different pH conditions (δ18O (VPDB): −6.4 ‰ to −7.9 ‰/(VSMOW): ‰ to +24.3 ‰) in comparison to the values observed in the shell parts grown under natural conditions, following the changes in .
The fractionation of carbon and oxygen isotopes between phases – brachiopod calcite and culture seawater – is defined as Δ13Ccal-DIC or Δ18O, where αcal-DIC/sw= [13C∕12C]cal/[13C∕12C]DIC or [18O∕16O]cal/[18O∕16O]sw, respectively. The calculated values based on our culture measurements are presented in Table 11.
For carbon isotopes, we observe variable Δ13Ccal-DIC between the different specimens and culturing treatments, and it is inconclusive whether this is linked to culturing conditions, differences between individuals or an ontogenetic component. It appears that there is about a 2 ‰ difference between the control specimen and samples from the acidification treatments (pH 7.35), with the last one being, strikingly, closer to the equilibrium with seawater DIC. Possibly, this illustrates the variability in kinetic effects (Bajnai et al., 2018), but may also be linked to changes in the source δ13CDIC in the control treatment. More studies are needed to fully answer this question.
Similarly, for oxygen isotopes, we find variable Δ18Ocal-sw with an apparent trend with pH. These values are offset from the equilibrium Δ18Ocal-sw (Δ18Ocal-sw = 32.9 at 10∘C) determined by Watkins et al. (2013, 2014). This suggests that M. venosa present non-equilibrium growth-rate-related isotope effects up to about −2.9 ‰, larger than the approx. −1.5 ‰ previously recorded by Bajnai et al. (2018). Provided that this offset can be constrained, brachiopods continue to present robust archives for palaeo-temperature reconstructions.
In summary, although it appears that variable growth rates present the most prominent confounding parameter complicating the interpretation of carbon and oxygen data, provided that we account for them, our results support the notion that brachiopods present robust geochemical archives, even when stressed by ocean acidification.
This study combines the analysis of shell microstructures on six specimens consisting of 1932 fibre size measurements, 170 primary layer thickness measurements, 256 punctal density and diameter measurements and stable isotope geochemistry on five specimens of 79 sample analyses, on brachiopods cultured under low-pH conditions for different time intervals. The results suggest the following conclusions.
In brachiopod specimens cultured for a period of 11 months, the microstructure produced by the specimen cultured at low pH (from pH 7.60 to pH 7.35) is different from that produced under control conditions (pH 8.00 and 8.15). In particular, the microstructure of shells produced at low pH tends to be more organic-rich, a result that lends strong support to brachiopod microstructure variations observed in fossil counterparts and the related effect of ocean acidification.
Brachiopod shell parts precipitated during culturing conditions of low pH for about 1 year record a change in the microstructure but not in the growth rate.
Their δ13C and δ18O values are rather constant during growth but experience a sharp drop during-culturing. In particular, the δ13C values dropped abruptly in specimens cultured for 1 year under low-pH conditions. This drop is related to the source of carbon dioxide gas used in the culture set-up.
Brachiopods are thus faithful recorders of the ambient carbon and oxygen isotope compositions, even when stressed by environmental perturbations such as ocean acidification.
The present observations are invaluable in using proxies and shell morphologic features for studying ocean acidification events and changes in atmospheric CO2 contents in the geologic past.
All data pertinent to this paper and its reported findings can be found in the paper itself or in the associated Supplement.
The supplement related to this article is available online at: https://doi.org/10.5194/bg-16-617-2019-supplement.
FY, LA and HJ designed the study and wrote the manuscript. FY prepared the specimens and carried out the microstructure analyses. HJ, UB, GC, and DŠ made the stable isotope measurements and/or helped with the interpretation of the data. HJ, DH and CH carried out the culturing experiments at GEOMAR, Kiel, and JL at AWI, Bremerhaven. JL provided M. venosa individuals from nature.
The authors declare that they have no conflict of interest.
This project was supported by the European Union's Horizon 2020 research and
innovation programme under Marie Skłodowska-Curie grant agreement no.
643084 (BASE–LiNE Earth). We would like to express our thanks to the
scientific divers and staff of Huinay Field Station, Chile, and Vreni
Häussermann is thanked for logistical support. We thank Nina Hörner
and Ulrike Holtz for help with culturing of the brachiopods at AWI, Dirk
Nürnberg at GEOMAR, Elena Ferrari (Università di Milano) for
technical support with stable isotope analyses, and Curzio Malinverno and
Agostino Rizzi (Università di Milano) for technical support with specimen
preparation and SEM analysis.
Edited by: David Gillikin
Reviewed by: Karem Azmy and one anonymous referee
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