Printer Friendly

IN SITU MEASUREMENTS OF pH, C[A.sup.2+], AND DIC DYNAMICS WITHIN THE EXTRAPALLIAL FLUID OF THE OCEAN QUAHOG ARCTICA ISLANDICA.

INTRODUCTION

Biomineralization is a regulated process within living organisms where calcium carbonate precipitates on an organic matrix (Crenshaw 1972a, Lowenstam 1981, Falini et al. 1996, Nudelman et al. 2006). Shell formation in bivalves (referred to as calcification throughout the following text) happens extracellularly with a strong biological control (Crenshaw 1980, Weiner & Traub 1980, Weiner & Dove 2003). There are different models on shell formation. (1) The shell is thought to form extracellularly from the extrapallial fluid (EPF) that is located between the inner shell surface and the outer mantle epithelium (OME) (Wada & Fujinuki 1976, Wilbur 1983, Addadi et al. 2003, Weiner & Dove 2003, Jacob et al. 2011). The OME is a thin barrier between the hemolymph and the EPF and is the secreting organ for the shell constituents. It is, hence, suggested to control the concentrations of inorganic ions (i.e., [Ca.sup.2+], [H.sup.+], and HC[O.sub.3.sup.-]) and organic components (i.e., proteins, glycoproteins, and polysaccharides) entering the EPF or the actual site of calcification (Crenshaw 1972a). (2) Within the mantle cells, vesicles with amorphous calcium carbonate (ACC) as a transient precursor of the crystalline aragonite or calcite form (Maria et al. 2002, Jacob et al. 2011). (3) Active cellular transport of CaC[O.sub.3] to the site of mineralization by hemocytes (Mount et al. 2004). Where the site of calcification is located and how CaC[O.sub.3] is exactly precipitated is the matter of ongoing research (Nudelman et al. 2007, Weiss 2010, Zhang et al. 2012).

The EPF is in direct contact with the shell and mostly divided in an inner and outer section (Wilbur 1983). The two compartments are divided by the pallial line where the OME is attached via numerous retractor muscles to the inner shell surface (Wilbur 1983, Wheeler 1992). Sampling of the fluid is difficult because of the small volumes, and analyses are mostly restricted to the inner EPF (Crenshaw 1972a, Wada & Fujinuki 1976, Gillikin et al. 2006, Ip et al. 2006).

Previous investigations of the EPF form a controversial picture of its organic and inorganic composition and ion transportation mechanisms. Regarding [Ca.sup.2+] concentration that has to be necessarily increased for CaC[O.sub.3] precipitation, only a little fraction of [Ca.sup.2+] was found freely dissolved within the EPF of the blue mussel Mytilus edulis (Misogianes & Chasteen 1979). Some organic molecules, such as an EPF glycoprotein, have been identified to reversely bind to [Ca.sup.2+], probably presenting a building block of the soluble organic shell matrix (Hattan et al. 2001). Coimbra et al. (1988) reported [Ca.sup.2+] concentrations within the EPF quite similar to seawater but with higher carbonate ion concentrations. The OME is highly permeable to [Ca.sup.2+], and different pathways for [Ca.sup.2+] transport through the mantle tissue have been discussed previously (Wheeler 1992, Klein et al. 1996, Gillikin et al. 2005, Carre et al. 2006).

The EPF is an enclosed compartment; thus, its chemistry can be well controlled, for example, by ion transport. It functions as a reservoir for all compounds necessary for calcification (Crenshaw 1972a, Misogianes & Chasteen 1979, Hattan et al. 2001). Several studies were dedicated to the EPF, but the concept of ion transportation mechanisms driving calcification is still controversial and the precise function of the EPF has yet stayed unresolved (Crenshaw 1972a, Carre et al. 2006, McConnaughey & Gillikin 2008, Thomsen et al. 2010).

Melzner et al. (2009) measured high pC[O.sub.2] values in extracellular fluids (in both hemolymph and EPF) that form a diffusion barrier for metabolic C[O.sub.2] excretion. Consequently, the pH values of the EPF are below that of ambient seawater for most of the time, and the fluid is undersaturated with respect to CaC[O.sub.3] (Crenshaw 1972a, Thomsen et al. 2010, Heinemann et al. 2012). Some bivalves can even calcify at high rates under acidified conditions of the surrounding seawater with a saturation state of CaC[O.sub.3] < 0.5 (Thomsen & Melzner 2010, Thomsen et al. 2010, Stemmer et al. 2013). The microenvironment in which calcification occurs has to be highly supersaturated with respect to shell minerals. Calcification is, thus, not likely to occur in the bulk of the EPF.

The species Arctica islandica (Linneaus, 1767), also called ocean quahog, was chosen as the study species because of its ecological significance and its important role as environmental proxy archive (Brey et al. 1990). The clam is a key species in Western Baltic benthic communities and flourishes in areas exposed to fluctuating environmental parameters as salinity, oxygen, and pC[O.sub.2] (Hansen et al. 1999). Stemmer et al. (2013) showed that shell growth was unaffected under elevated C[O.sub.2] levels. The present study helps to clarify the role of the EPF in the calcification process within young specimen of the ocean quahog by directly measuring ion dynamics with high temporal resolution. Optical pH measurements were performed within the inner EPF, and pH and [Ca.sup.2+] microsensors were used to measure short- and long-term dynamics. Dissolved inorganic carbon (DIC) was also measured over time to evaluate the internal carbonate system of the EPF. The data are used to discuss the function of the EPF as a shielded site for calcification.

MATERIALS AND METHODS

Clam Maintenance and Preparation

All measurements were conducted on the North Atlantic bivalve Arctica islandica. Young bivalves were collected from Kiel Bight in the Western Baltic and maintained in aquaria at 14[degrees]C and a salinity of 25. Seawater was exchanged every 2 days. As a food source, live marine plankton (SA/DT's Premium Blend; Sustainable Aquatics, Jefferson City, TN) was added every 2 days.

For microsensor measurements, holes were drilled in the bivalve shell of one specimen using a hand held drill (Dremel "MultiPro" 395; Germany). The first layers of the outer shell were removed carefully with a polishing tool in the area before or behind the pallial line and between the adductor muscles depending on the compartment of interest. Preventing heating of the shell and accumulation of CaC[O.sub.3] powder, the shell was flushed constantly with a water stream. When the shell at the target area was thin enough, a small drilling head was used. Carefully three holes of ~2 mm in diameter were drilled into the bivalve shell: two entrances for the microsensors ([Ca.sup.2+] and pH) and one entrance for the reference electrode.

The holes were extended and sealed by gluing pipette tips of ~10 mm length onto the holes. To prevent gas exchange, parafilm was applied to seal the pipette tips (further referred to as catheters, Fig. 1).

For microscopic pH measurements, a PVC measuring window (with an area of ~ 1 [cm.sup.2]) was attached onto a similarly drilled opening of the shell of two different specimens (Fig. 1A). The pH indicator was injected into the EPF through a catheter in the window that was then sealed with parafilm.

Clams were positioned in the experimental chambers and holding tanks so that catheters were above the seawater level at all times (Fig. 1). After shell preparation, the clams were acclimatized in the holding tanks for more than 12 h before measurements commenced. All bivalves were actively filtrating shortly after preparation. The bivalves were checked for tissue damages after measurement.

Microscopic pH Analysis

For microscopic analysis, a pH-sensitive nonmembrane-permeable dye BCECF-dextran (Invitrogen) was dissolved just before the measurement (2 g/L). Fifty microliters was injected in the inner EPF. The excitation intensity ratio (Invitrogen Manual) of BCECF at 458 and 488 nm (emission: 505-550 nm) alters with changing pH, thus enabling measurements independent from the dye concentration. Fluorescence measurements were carried out with an upright confocal microscope (LSM 510; Zeiss, Oberkochen, Germany) using an argon laser (458 and 488 nm, blue light) for excitation of the indicator dye. Fluorescence emission was measured between 505 and 550 nm.

By integrating the measured intensities of each image of a stack, a pH depth profile between the installed window (hereafter referred to as "shell") and the OME of the animal was calculated. Calibrations were performed using BCECF in seawater with pH 8.85 and pH 5.75 (Invitrogen Manual). Optical sections of extracellular pH of the clam were taken in 50-[micro]m steps every 5.6 sec. Parameters of the measurement series are listed in Table 1.

The window was clearly visible when in focus, because of its autofluorescence, and defined as the zero depth. The end point (meaning the OME was reached) was defined when fluorescence signals decreased down to the dimension of the signal offset, as the dye molecules cannot penetrate membranes and tissues.

During measurements, the bivalves were placed in a petri dish submerged in seawater. Only the installed window was positioned above the surface. By adding cooled water several times during the measurements, the seawater temperature was kept around 14[degrees]C with a salinity of 25. During all measurements, the bivalves were open and filtrating.

Microsensor Measurements

Liquid ion exchange membrane-type pH and [Ca.sup.2+] microelectrodes were built and calibrated as described previously (de Beer et al. 1997, de Beer 2000). All pH measurements were performed on the NBS scale. Microsensors had a tip diameter of approximately 10 [micro]m and were installed on a micromanipulator (MD 4; Maerzhaeuser, Wetzlar, Germany) fixed on a heavy stand to enable careful positioning within the installed tubes on the clam to reach the EPF. The clam was submerged and the installed catheters were reaching out of the water covered by parafilm. A polycarbonate flow chamber ensured the circulation with aerated seawater at constant temperature of 14[degrees]C and a salinity of 25. The experimental setup is depicted in Figure 2.

Electrodes were guided carefully through the punctured parafilm of each catheter. The reference electrode was first fixed within one catheter with the tip of the reference reaching shortly behind the shell into the EPF. The fluid reached about 1-2 mm into the catheters so that contact of the sensors with the fluid was ensured. Positioning of the microsensors was performed manually with the help of a stereoscope. Measurement depth was determined by monitoring pH gradients while inserting sensors into the catheters. pH signals remained constant less than 300 [micro]m depth within the bivalve shell (Fig. 1). This depth range was chosen for all long-term time series measurements.

Signals of pH and [Ca.sup.2+] were recorded simultaneously every 3-10 sec. pH and [Ca.sup.2+] values were taken before and after the measurements from the experimental seawater and used as baselines for calculations of the [DELTA]pH and [DELTA][Ca.sup.2+] in the EPF of Arctica islandica. All measurements were conducted under ambient light conditions.

Dissolved Inorganic Carbon Measurements

Extrapallial fluid samples were taken during microsensor measurements using gastight glass syringes (Hamilton). A volume of at least 80 [micro]L of the EPF was carefully drawn from the installed catheters with a fine needle syringe and immediately transferred to a DIC analyzer. Levels of DIC were quantified by flow injection analysis (Hall & Aller 1992). This procedure was repeated over the course of one measurement as long as sufficient EPF was accessible.

Calcite Saturation Calculation

We used C02SYS (Lewis & Wallace 1998) to calculate the saturation of calcite ([OMEGA]), from the DIC (assuming a seawater DIC of 2,300 [micro]mol/kg) and the measured pH.

RESULTS

The transparent (PVC) window in the shell enabled optical measurements of pH depth profiles between the OME and the shell. Insertion of [Ca.sup.2+] and pH microsensors into the EPF through small operational holes was successful, and synchronous recordings of [Ca.sup.2+] and pH were possible with high temporal resolution.

Optical pH Measurements

Using BCECF-dextran as a pH indicator, it was possible to measure a pH gradient over depth within the inner EPF of Arctica islandica between the shell and the OME of the animal. All pH depth profiles of specimen #1 and the first 17 depth profiles of specimen #2 show a decrease in pH toward the OME. These measurements show that the pH at the OME surface is very low over a long period of time, probably because of respiration. These profiles were averaged and are displayed in Figure 3.

On several occasions, the pH at the OME increased strongly (Fig. 4). The last 11 pH depth profiles of specimen #2 show an inversion of a decreasing to an increasing pH gradient toward the OME (Fig. 4). The pH at the shell did not follow the OME pH dynamics but was comparatively constant. At the observed pH of ~9.5, the supersaturation of CaC[O.sub.3] was calculated with CO2SYS. Assuming a DIC of 2,300 [micro]mol/kg (seawater DIC), the oversaturation was 30-fold.

Simultaneous pH, [Ca.sup.2+], and DIC Dynamics

Using liquid ion exchange microsensors, pH and [Ca.sup.2+] concentrations were measured in situ and simultaneously within the inner EPF of Arctica islandica while the valves of the calm were open. Both values change synchronously over time. Rising pH values are accompanied by increasing [Ca.sup.2+] levels and vice versa (Fig. 5). Occasionally, the synchronous dynamics change and move in opposite directions. Measurements were performed every 3 sec and demonstrate the fast change of the two parameters.

Simultaneous microsensor long-term measurements of pH and [Ca.sup.2+] within the inner EPF of Arctica islandica were performed over 7 h. The valves of the clam were open over the whole period of time. pH of the EPF was between 0.2 and 0.6 units lower than that of the surrounding seawater. Calcium ion concentrations increased up to 2.5 mM over seawater [Ca.sup.2+] concentrations (see [DELTA][Ca.sup.2+] in Fig. 6A). During this microsensor measurement, EPF samples were analyzed for DIC. Interestingly, DIC values also oscillate but are not synchronous to pH and [Ca.sup.2+] (Fig. 6B).

Dissolved inorganic carbon was measured six times during the microsensor measurements, and the difference to the surrounding experimental seawater was calculated. The dynamics of [DELTA]DIC can be seen in Figure 6B. During the first 2 h of the measurements (with increasing pH and [Ca.sup.2+] level), the DIC concentration is similar to that in seawater with a slightly lower DIC concentration of ~174 [micro]mol/kg. The following three measurements show a steep increase in DIC of up to 3,191 [micro]mol/kg, which exceeds the seawater DIC level by more than 50%. During elevated DIC levels, the two other parameters, pH and [Ca.sup.2+], show a simultaneous oscillation. The last measured DIC value had reversed to almost seawater values.

DISCUSSION

For the detailed understanding of the shell-formation process, mechanisms of ion transportation to the site of calcification need to be identified (Carre et al. 2006, McConnaughey & Gillikin 2008). In bivalve shell formation, the two major compartments filled with the inner and the outer EPF are closest to the site of biomineralization (Wheeler 1992). The outer EPF, however, is not suitable for analysis because of the small area and volume. Therefore, this study focused on the inner EPF.

The number of observations was limited to one set of extensive microsensor measurements (pH and calcium) and two series of optical pH measurements as the procedures to get access to the EPF were difficult and appeared often stressful for the animal.

The exact series of the calcification mechanisms are still debated. One increasingly accepted scenario is that ACC is transported in vesicles to the site of calcification, where the unstable ACC is converted into calcite (Addadi et al. 2003). The ACC could be stabilized before reaching the site of calcification by [Mg.sup.2+], phosphate, or organics (Weiner et al. 2005). Alternatively, metabolically driven membrane transporters pump [Ca.sup.2+] to the site of calcification, or exchangers transport [H.sup.+] from, and [Ca.sup.2+] into the calcifying site, leading to an increase in [Ca.sup.2+] and pH, thus stimulating calcite formation (Al-Horani et al. 2003a, 2003b). The latter exchange process is possibly controlled by a Ca-H-ATPase. Several mechanisms in parallel or in combination are possible. For example, ACC may be transported in vesicles and, during its release on the calcifying site, the pH is elevated by active [H.sup.+] pumps. This study shows the occurrence of pumping and does not exclude the ACC vesicle mechanism.

The low pH recorded at the tissue surface may be well driven by respiratory C[O.sub.2] production. The two clams had slightly different pH values at the epithelium surface, but the profiles were similar in shape. The pH decrease in the EPF through activity by the tissue will decrease the calcite oversaturation and hence reduce calcification. The sudden elevation of the pH from 7.3 to levels of above 9.5 in less than 20 min were most likely caused by active [H.sup.+] uptake by the epithelium, which costs metabolic energy. Calcification will be accelerated during such an alkalinization event. This observation suggests that calcification is not a continuous process but occurs in bursts. Possibly, this explains the pattern of bands in the shells.

The simultaneously recorded pH and [Ca.sup.2+] concentration showed a parallel dynamic (Fig. 5), which can be explained by a [Ca.sup.2+]/[H.sup.+] exchanger ([Ca.sup.2+]-ATPase). Such a counterporter is thought to drive calcium carbonate precipitation (Al-Horani et al. 2003, McConnaughey & Gillikin 2008).

Indeed, Ca-H-ATPase can transport [Ca.sup.2+] across the mantle epithelia to the EPF in exchange for 2[H.sup.+] (Schwiening et al. 1993). Their activity was shown to induce synchronous [Ca.sup.2+] and pH dynamics at the surface of macroalgae (McConnaughey & Falk 1991). These transporters have been described in detail and are suggested to play a role in the calcification process (Kingsley & Watabe 1985, Ip & Lim 1991). Moreover, Fan et al. (2007) found evidence for [Ca.sup.2+] -ATPase on the OME of pearl oysters. Interestingly, similar pH and [Ca.sup.2+] dynamics were measured in the calcification site of coral polyps, the calicoblastic fluid (Al-Horani et al. 2003a, 2003b). The authors validated the activity of [Ca.sup.2+] -ATPase enzyme via [Ca.sup.2+] -ATPase inhibitors.

The sudden increase in DIC of 1 mM within 10 min, followed by an equally large decrease 2.5 h later cannot be explained by respiratory activity. As the oxygen level will not exceed 0.3 mM, the DIC production in the EPF cannot exceed 0.3 mM, in the unlikely case that complete oxygen depletion could occur. Rather, an active pumping of DIC toward the calcifying site can explain this increase. Possibly, a sudden release of ACC vesicles occurred. Like the sudden alkalinization of the EPF, the DIC dynamics hint to bursts of calcification. The pH dynamics, measured at the same time with a pH microsensor, show a sudden decrease of 0.3 units. Taking the two observations together, a pH increase is coupled to a DIC decrease and vice versa. Despite the increase in DIC, during the acidification period, the [OMEGA] (CaC[O.sub.3]) decreases from 3.6 to 2.7. It can only be speculated on the processes that control the DIC dynamics, but these data suggest a correlation between DIC and [H.sup.+]/[Ca.sup.2+] pumping.

This study proposes that these pumps are involved in shell formation, possibly together with ACC vesicles. The [H.sup.+] pumps can induce a pH at the tissue surface that is high enough to induce calcification, but the pH close to the shell surface of the inner EPF stays too low (Fig. 3). The oversaturation of 30-fold is certainly enough to drive calcite formation. It is documented that CaC[O.sub.3] precipitation only occurs under strong local supersaturation. For example, in calcifying algae, supersaturation was recorded greater than 30-fold (McConnaughey & Falk 1991), in freshwater stromatolites, it was greater than 20-fold (Bissett et al. 2008), and in corals and hypersaline microbial mats ~25-fold (Al-Horani et al. 2003b, Ludwig et al. 2005). The authors of this study propose that calcification happens when the tissue is in close contact with the shell, as, for example, in the outer EPF. Here, the distance is in the order of microns, and in this enclosed volume, the water chemistry can even be better controlled to induce calcification. The pumping may offer the organism several options to control the shell building. First, the pumps may be actively regulated, like in other complex organisms. Second, the animal may control the distance between shell and tissue in which the active pumps are located (OME). Probably, the mechanisms regulate [H.sup.+], [Ca.sup.2+], and DIC by membrane transporters and possibly ACC vesicles that are concentrated in the area where the shell grows. The calcification will be most important at the shell margin where shell expansion occurs; however, according to the data, these pumps are also present in the OME adjacent to the inner EPF where calcification leads to increased shell thickness.

CONCLUSION

In the present study, the inner EPF of Arctica islandica was investigated as a highly dynamic compartment with regard to pH, [Ca.sup.2+], and DIC. A sudden increase in pH from below 7 up to 9.5 at the OME shows active [H.sup.+] pumping and is consistent with the hypothesis of [H.sup.+] pumps being integrated in the OME. Simultaneous pH and [Ca.sup.2+] microsensor measurements revealed remarkable short-term dynamics and demonstrate the power of this method for in situ measurements of ion dynamics. The function of this active pumping process likely plays a role in the calcification process. Calculations of the saturation state within the inner EPF indicate an environment that can reach very strong CaC[O.sub.3] oversaturation within limited portions near the OME. The animal might temporally shift the OME toward the growing shell surface to permit calcification.

Future in situ investigations of the OME in the inner and in the outer EPF using [Ca.sup.2+] markers will help to uncover possible [Ca.sup.2+] pumps or channels and get us closer to resolve the enigma of the biomineralization process within Arctica islandica.

ACKNOWLEDGMENTS

Many thanks to the technicians of the microsensor group for technical support. We also would like to thank Duygu Sevilgen, Gisela Lannig, and Christian Bock for fruitful discussions. Thanks to Eva Philipp for organizing the cruise where the animals were collected. This research was funded by the Alfred Wegener Institute in the framework of the BIOACID project and the Max Planck Institute for Marine Microbiology.

LITERATURE CITED

Addadi. L., S. Raz & S. Weiner. 2003. Taking advantage of disorder: amorphous calcium carbonate and its roles in biomineralization. Adv. Mater. 15:959-970.

Al-Horani, F. A., S. M. Al-Mograbi & D. de Beer. 2003a. The mechanism of calcification and its relation to photosynthesis and respiration in the scleractinian coral Galaxea fascicularis. Mar. Biol. 142:419-426.

Al-Horani, F. A., S. M. Al-Mograbi & D. de Beer. 2003b. Microsensor study of photosynthesis and calcification in the scleractinian coral Galaxea fascicularis: active internal carbon cycling. J. Exp. Mar. Biol. Ecol. 288:1-15.

Bissett, A., D. de Beer, R. Schoon, A. Reimer & G. Arp. 2008. Microbial mediation of stromatolite formation in karst-water creeks. Limnol. Oceanogr. 53:1159-1168.

Brey, T., W. E. Arntz, D. Pauly & H. Rumohr. 1990. Arctica (Cyprina) islandica in Kiel Bay (Western Baltic)--growth, production and ecological significance. J. Exp. Mar. Biol. Ecol. 136:217-235.

Carre, M., I. Bentaleb, O. Bruguier, E. Ordinola, N. T. Barrett & M. Fontugne. 2006. Calcification rate influence on trace element concentrations in aragonitic bivalve shells: evidences and mechanisms. Geochim. Cosmochim. Acta 70:4906-1920.

Coimbra, J., J. Machado, P. L. Fernandes, H. G. Ferreira & K. G. Ferreira. 1988. Electrophysiology of the mantle of Anodonta cygnea. J. Exp. Biol 140:65-88.

Crenshaw, M. A. 1972a. The inorganic composition of molluscan extrapallial fluid. Biol. Bull. 143:506-512.

Crenshaw, M. A. 1972b. The soluble matrix from Mercenaria mercenaria shell. Biomineral. Res. Rep. 6:6-11.

Crenshaw, M. A. 1980. Mechanisms of shell formation and dissolution. Top. Geobiol. 1:115-132.

de Beer, D. 2000. Potentiometric microsensors for in situ measurements in aquatic environments. In: Buffle, J. & G. Horvai, editors. In situ monitoring of aquatic systems: chemical analysis and speciation. London, United Kingdom: Wiley & Sons. pp. 161-194.

de Beer, D., A. Schramm, C. M. Santegoeds & M. Kuhl. 1997. A nitrite microsensor for profiling environmental biofilms. Appl. Environ. Microbiol. 63:973-977.

Falini, G., S. Albeck, S. Weiner & L. Addadi. 1996. Control of aragonite or calcite polymorphism by mollusc shell macromolecules. Science 271:67-69.

Fan, W., C. Li, S. Li, Q. Feng, L. Xie & R. Zhang. 2007. Cloning, characterization, and expression patterns of three sarco/endoplasmic reticulum [Ca.sup.2+] -ATPase isoforms from pearl oyster (Pinctada fucata). Acta Biochim. Biophys. Sin. (Shanghai) 39:722-730.

Gillikin, D. P., F. Dehairs, A. Lorrain, D. Steenmans, W. Baeyens & L. Andre. 2006. Barium uptake into the shells of the common mussel (Mytilus edulis) and the potential for estuarine paleo-chemistry reconstruction. Geochim. Cosmochim. Acta 70:395-407.

Gillikin, D. P., A. Lorrain, J. Navez, J. W. Taylor, E. Keppens, W. Baeyens & F. Dehairs. 2005. Strong biological controls on Sr/Ca ratios in aragonitic marine bivalve shells. Geochem. Geophys. Geosyst. 6:Q05009.

Hall, O. J. & R. C. Aller. 1992. Rapid, small-volume, flow injection analysis for SC[O.sub.2] and [NH.sub.4.sup.+] in marine and freshwaters. Limnol. Oceanogr. 37:1113-1119.

Hansen, H. P., H. C. Giesenhagen & G. Behrends. 1999. Seasonal and long-term control of bottom-water oxygen deficiency in a stratified shallow-water coastal system. ICES J. Mar. Sci. 56:65-71.

Hattan, S. J., T. M. Laue & N. D. Chasteen. 2001. Purification and characterization of a novel calcium-binding protein from the extrapallial fluid of the mollusc, Mytilus edulis. J. Biol. Chem. 276:4461-4468.

Heinemann, A., J. Fietzke, F. Melzner, F. Boehm, J. Thomsen, D. Garbe-Schoenberg & A. Eisenhauer. 2012. Conditions of Mytilus edulis extracellular body fluids and shell composition in a pH-treatment experiment: acid-base status, trace elements and [[delta].sup.11] B. Geochem. Geophys. Geosyst. 13:1-17.

Ip, Y. K. & A. L. L. Lim. 1991. Are calcium and strontium transported by the same mechanism in the hermatypic coral Galaxea fascicularis. J. Exp. Biol. 159:507-513.

Ip, Y. K., A. M. Loong, K. C. Hiong, W. P. Wong, S. F. Chew, K. Reddy, B. Sivaloganathan & J. S. Ballantyne. 2006. Light induces an increase in the pH of and a decrease in the ammonia concentration in the extrapallial fluid of the giant clam Tridacna squamosa. Physiol. Biochem. Zool. 79:656-664.

Jacob, D. E., R. Wirth, A. L. Soldati, U. Wehrmeister & A. Schreiber. 2011. Amorphous calcium carbonate in the shells of adult Unionoida. J. Struct. Biol. 173:241-249.

Kingsley, R. J. & N. Watabe. 1985. Ca-ATPase localization and inhibition in the gorgonian Leptogorgia virgulata (Lamarck) (Coelenterata: Gorgonacea). J. Exp. Mar. Biol. Ecol. 93:157-167.

Klein, R. T.. K. C. Lohmann & C. W. Thayer. 1996. Sr/Ca and C-13/C-12 ratios in skeletal calcite of Mytilus trossulus: covariation with metabolic rate, salinity, and carbon isotopic composition of seawater. Geochim. Cosmochim. Acta 60:4207-4221.

Lewis, E. & D. W. R.Wallace. 1998. Program developed for C[O.sub.2] system calculations. ORNL/CDIAC-105. Oak Ridge, TN: Oak Ridge National Laboratory.

Lowenstam, H. A. 1981. Minerals formed by organisms. Science 211:1126-1131.

Ludwig, R., F. A. Al-Horani, D. de Beer & H. M. Jonkers. 2005. Photosynthesis controlled calcification in a hypersaline microbial mat. Limnol. Oceanogr. 50:1836-1843.

Maria, W. I., T. Noreen, A. Lia & W. Steve. 2002. Mollusc larval shell formation: amorphous calcium carbonate is a precursor phase for aragonite. J. Exp. Zool. 293:478-491.

McConnaughey, T. A. & R. H. Falk. 1991. Calcium-proton exchange during algal calcification. Biol. Bull. 180:185-195.

McConnaughey, T. A. & D. P. Gillikin. 2008. Carbon isotopes in mollusk shell carbonates. Geo-Mar. Lett. 28:287-299.

Melzner, F., M. A. Gutowska, M. Hu & M. Stumpp. 2009. Acid-base regulatory capacity and associated proton extrusion mechanisms in marine invertebrates: an overview. Comp. Biochem. Physiol. 153A:S80.

Misogianes, M. J. & N. D. Chasteen. 1979. Chemical and spectral characterization of the extrapallial fluid of Mytilus edulis. Anal. Biochem. 100:324-334.

Mount, A. S., A. P. Wheeler, R. P. Paradkar & D. Snider. 2004. Hemocyte-mediated shell mineralization in the eastern oyster. Science 304:297-300.

Nudelman, F., H. H. Chen, H. A. Goldberg, S. Weiner & L. Addadi. 2007. Spiers memorial lecture: lessons from biomineralization: comparing the growth strategies of mollusc shell prismatic and nacreous layers in Atrina rigida. Faraday Discuss. 136:9-25.

Nudelman, F., B. A. Gotliv, L. Addadi & S. Weiner. 2006. Mollusk shell formation: mapping the distribution of organic matrix components underlying a single aragonitic tablet in nacre. J. Struct. Biol. 153:176-187.

Schwiening, C. J., H. J. Kennedy & R. C. Thomas. 1993. Calcium hydrogen-exchange by the plasma-membrane Ca-ATPase of voltage-clamped snail neurons. Proc. Biol. Sci. 253:285-289.

Stemmer, K., G. Nehrke & T. Brey. 2013. Elevated C[O.sub.2] levels do not affect the shell structure of the bivalve Arctica islandica from the Western Baltic. PLoS One 8:e70106.

Thomsen, J., M. A. Gutowska, J. Saphoerster, A. Heinemann, K. Truebenbach, J. Fietzke, C. Hiebenthal, A. Eisenhauer, A. Koertzinger, M. Wahl & F. Melzner. 2010. Calcifying invertebrates succeed in a naturally C[O.sub.2]-rich coastal habitat but are threatened by high levels of future acidification. Biogeosciences 7:3879-3891.

Thomsen, J. & F. Melzner. 2010. Moderate seawater acidification does not elicit long-term metabolic depression in the blue mussel Mytilus edulis. Mar. Biol. 157:2667-2676.

Wada, K. & T. Fujinuki. 1976. Biomineralization in bivalve molluscs with emphasis on the chemical composition of the extrapallial fluid. In: Watabe, N. & K. M. Wilbur, editors. The mechanism of mineralization in the invertebrates and plants. Univ. South Carolina Press. pp. 175-190.

Weiner, S. & P. Dove. 2003. An overview on biomineralization processes and the problem of the vital effect, vol. 54. In: Dove, P. M., S. Weiner & J. J. De Yoreo, editors. Biomineralization. Washington, DC: Mineralogical Society of America. pp. 1-31.

Weiner, S., I. Sagi & L. Addadi. 2005. Choosing the crystallization path less traveled. Science 309:1027-1028.

Weiner, S. & W. Traub. 1980. X-ray-diffraction study of the insoluble organic matrix of mollusk shells. FEBS Lett. 111:311-316.

Weiss, I. M. 2010. Jewels in the pearl. Chembiochem 11:297-300.

Wheeler, A. P. 1992. Mechanisms of molluscan shell formation. In: Bonucci, E., editor. Calcification in biological systems. Boca Raton, FL: CRC Press. pp. 179-215.

Wilbur, K. M. & A. S. M. Saleuddin. 1983. Shell formation. In: The mollusca, vol. 4. Physiology. Wilbur, K. M. & A. S. M. Saleuddin, editors. New York, NY: Academic Press. pp. 235-287.

Zhang, G., X. Fang, X. Guo, L. Li, R. Luo, F. Xu, P. Yang, L. Zhang, X. Wang, H. Qi, Z. Xiong, H. Que, Y. Xie, P. W. H. Holland, J. Paps, Y. Zhu, F. Wu, Y. Chen. J. Wang, C. Peng, J. Meng, L. Yang, J. Liu, B. Wen, N. Zhang, Z. Huang, Q. Zhu, Y. Feng, A. Mount, D. Hedgecock, Z. Xu, Y. Liu, T. Domazet-Loso, Y. Du, X. Sun, S. Zhang, B. Liu, P. Cheng, X. Jiang, J. Li, D. Fan, W. Wang, W. Fu, T. Wang, B. Wang. J. Zhang, Z. Peng, Y. Li, N. Li, J. Wang, M. Chen, Y. He, F. Tan, X. Song, Q. Zheng, R. Huang, H. Yang, X. Du, L. Chen, M. Yang, P. M. Gaffney, S. Wang, L. Luo, Z. She, Y. Ming, W. Huang, S. Zhang, B. Huang, Y. Zhang, T. Qu, P. Ni, G. Miao, J. Wang, Q. Wang, C. E. W. Steinberg, H. Wang, N. Li, L. Qian, G. Zhang, Y. Li, H. Yang, X. Liu, J. Wang. Y. Yin & J. Wang. 2012. The oyster genome reveals stress adaptation and complexity of shell formation. Nature 490:49-54.

KRISTINA STEMMER, (1,2*[dagger]) THOMAS BREY, (1,3) MARTIN S. GUTBROD, (2) MARTIN BEUTLER, (4) BURGEL SCHALKHAUSSER (1) AND DIRK DE BEER (2)

(1) Alfred-Wegener-Institute Helmholtz Centre for Polar and Marine Research, Am Handelshafen 12, Bremerhaven D-27570, Germany; (2) Max-Planck-Institute for Marine Microbiology, Celsiusstra[beta]e 1, Bremen D-28359, Germany; (3) Helmholtz Institute for Functional Marine Biodiversity at the University Oldenburg, Ammerlander Heerstra[beta]e 231, Oldenburg D-26129, Germany; (4) bionsys Gmb H, Fahrenheitstra[beta]e 1, Bremen D-28359, Germany

([dagger]) Present address: Kristina Stemmer, PhD, Zeughausstrasse 81, 3902 Glis, CH.

(*) Corresponding author. E-mail: kristina.stemmer@gmx.de

DOI: 10.2983/035.038.0107
TABLE 1.
Parameters for microscopic pH.

Specimen   Stack   No. of   Steps        Total       Time per
           size    stacks   ([micro]m)   distance    measurement (s)
                                         ([micro]m)

#1         32      13       50           1,600       5.6
#2         24      28       50           1,200       5.6

Specimen   Time between     Total
           each stack (s)   time (min)

#1         600              358.83
#2         300              197.72

Parameters used for microscopic pH measurements within the inner EPF of
two specimens of Arctica islandica. The stack size comprises the amount
of measurement points. Several stacks have been measured consecutively
(No. of stacks).
COPYRIGHT 2019 National Shellfisheries Association, Inc.
No portion of this article can be reproduced without the express written permission from the copyright holder.
Copyright 2019 Gale, Cengage Learning. All rights reserved.

Article Details
Printer friendly Cite/link Email Feedback
Author:Stemmer, Kristina; Brey, Thomas; Gutbrod, Martin S.; Beutler, Martin; Schalkhausser, Burgel; De Beer
Publication:Journal of Shellfish Research
Article Type:Report
Date:Apr 1, 2019
Words:5455
Previous Article:ARTIFICIAL SELECTION AND SIZE AT FIRST SEXUAL MATURITY OF PERNA PERNA MUSSELS (LINNAEUS, 1758) IN SOUTHEASTERN BRAZIL.
Next Article:SEASONAL DNA METHYLATION VARIATION IN THE FLAT TREE OYSTER ISOGNOMON ALATUS FROM A MANGROVE ECOSYSTEM IN NORTH BISCAYNE BAY, FLORIDA.
Topics:

Terms of use | Privacy policy | Copyright © 2022 Farlex, Inc. | Feedback | For webmasters |