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Recent field experiments have identified the need for accurate metabolic measurements on coral reefs at short time intervals in order to detect subtle aspects such as phase lags between the concentrations and flux rates of major metabolic parameters over the diurnal cycle (e.g., Shamberger et al., 2011; McMahon et al., 2013). There is a need to test the assumption that night calcification is very low and constant and that calcification is limited by inorganic carbon concentration in the form of CO32−. Finely detailed diurnal metabolic measurements are difficult to obtain in field investigations. For example, Falter et al. (2012) based their extensive study at Nigaloo Reef, NW Australia on a total of 13 summer measurements of calcification taken at various times over 12 days between 08:00 and 18:00 with one night measurement at 21:00. The following winter a total of 11 more measurements were made over 4 days with no night measurements. These data are valuable, but do not provide the diurnal resolution that is needed to fully describe coral and coral reef metabolism. Thus we undertook a laboratory investigation that would provide such data.

Background Information

The term Ωarag is defined as: Ωarag=Ca2+CO32Ksp where Ksp is the solubility constant of aragonite. The [Ca2+] in normal present-day oceanic seawater is essentially constant at 10.3 mmol kg−1 SW, normalized to salinity. Likewise, Ksp is a constant (at a given temperature, pressure, and salinity), so in shallow oceanic waters Ωarag is directly proportional to [CO32−]. Changes in seawater pH shift the equilibria between the various forms of dissolved inorganic carbon (DIC) as follows: CO2+H2OH++HCO32H++CO32. Calcification inevitably produces an excess of H+ and thus reduces total alkalinity (AT) by two moles for every mole of CaCO3 precipitated (Kinsey, 1978; Smith & Kinsey, 1978). The correct equations for calcification are as follows: Ca2++CO2+H2OCaCO3+2H+ Ca2++H++HCO3CaCO3+2H+ Ca2++2H++CO32CaCO3+2H+ Equations 35 are written in two dimensions with a red arrow showing the relationship between the carbonate species (in parentheses) that shift with the changes in [H+] described as Eq. (2). Dissolution is the reverse of the calcification reaction. Net calcification (Gnet) is the sum of calcification (positive flux) and dissolution (negative flux). When the equations are written correctly in this manner the importance of protons becomes apparent with two moles of H+ produced for every mole of CaCO3 precipitated regardless of which form of dissolved inorganic carbon (DIC) is involved.

The following equations describe photosynthetic carbohydrate formation from the various available CO2 species: CO2+H2OCH2O+O2 H++HCO3CH2O+O2 2H++CO32CH2O+O2. The photosynthesis equations are also written in two dimensions with the red arrows showing changes in distribution of species that occurs (Eq. (2)) with shifts in pH. Note that photosynthesis increases pH (lowers [H+]) while the reverse reaction of respiration decreases pH (increases [H+]). Net photosynthesis (Pnet) is the sum of photosynthesis (positive flux) and respiration (negative flux). Unlike calcification-dissolution, photosynthesis-respiration does not alter total alkalinity (AT).

In sum, photosynthesis and calcification both lower the seawater DIC, while respiration and CaCO3 dissolution raise DIC. Only the precipitation or dissolution of CaCO3 significantly alters AT. Consequently, changes in [AT] can be used to calculate calcification and dissolution rates (Gnet), and is widely used in this regard. Photosynthesis and respiration can radically alter [H+] and thus can alter relative concentration of CO32−,HCO3 and CO2. Coral calcification is a biological process that is heavily influenced by the associated processes of photosynthesis and respiration (Pnet) that modify pH. Protons can be considered a waste product of calcification Eqs. (3)(5) and O2 a waste product of photosynthesis Eqs. (6)(8).

Methods and Materials

A mesocosm experiment was undertaken in order to precisely measure the changes in bulk sea water chemistry and material flux caused by coral and algae metabolism over a diurnal cycle. The experiment was conducted in the flow-through mesocosm system at the Hawaii Institute of Marine Biology, Kaneohe Bay, Oahu, Hawaii. The mesocosm system has been described previously in detail (Jokiel et al., 2008; Andersson et al., 2009; Jokiel, Bahr & Rodgers, in press). The fiberglass mesocosm tanks were located in full sunlight and supplied with flowing seawater pumped from approximately 2 m depth at the edge of the Coconut Island coral reef. Each mesocosm received a flow of approximately 7.5 to 8.5 l min−1 resulting in a turnover rate of approximately 1 h. Solar input at the site was monitored with a LiCor Brand Quantameter (Li-Cor Inc., Lincoln, NE, USA), which measured photosynthetically active radiance (PAR) between 400 nm and 700 nm.

Three continuous flow mesocosms were used for this experiment. The first mesocosm (“Coral only”) was loaded with 7.6 kg buoyant weight of the reef coral Montipora capitata for close to 100% coverage of the bottom (Table 1). This buoyant weight translates into 11.5 kg dry skeletal weight (Jokiel, Maragos & Franzisket, 1978). The second mesocosm (“Coral plus Algae”) contained the same weight of live coral plus 3.1 kg wet weight of the macroalgae Gracillaria salicornia. The third mesocosm (“Algae only”) was loaded with the same weight of the macroalgae. A small biomass of calcifying organisms was present on the macroalgae in the form of epiphytes that were not removed. Dead skeletal material and sediment were excluded from all three mesocosms to reduce the complicating effect of decalcification of carbonates and related processes on Gnet (Murillo, Jokiel & Atkinson, 2014). The organisms in the mesocosms were allowed to acclimate to mesocosm conditions for one week prior to the experiment.

Table 1:
Mesocosm volume and biomass of the coral Montipora capitata and the macroalgaGracillaria salicornia.
Tank dimensions in cm
Mesocosm Biomass Length Width Water depth Volume (l)
Coral only 7,555 g buoyant weight coral 117 117 38 520
Coral plus Algae 7,555 g buoyant weight coral, and
3,151 g of Gracillaria salicornia
117 117 38 520
Algae 3,151 g of Gracillaria salicornia 117 117 35 479
DOI: 10.7717/peerj.378/table-1

This experimental design allows the three treatments to be run simultaneously which eliminates the between-treatment variance due to solar irradiance, temperature and other factors that would occur if they were run at different times. The functioning of each community under identical conditions serves as a control and as a contrast to the other two communities. Response of these communities to the diurnal irradiance cycle and variation in other factors is non-linear, so the data were analyzed by graphical comparison and integrated response of 24 h Pnet and Gnet.

The seawater inflow enters at the bottom in the center of each mesocosm (see Smith et al., 1977 for details on the mesocosm system) at a vertical angle, which ensures a uniform and well-mixed system. Maintaining seawater inflow of reef water at constant rates insured that natural fluctuations in seawater chemistry observed on the adjacent reef during the diel cycle was preserved during the experiment. Water chemistry was sampled hourly from 06:00 on 24 April to 07:00 on 25 April 2012 at the inlet and outlet and the flow rate recorded. During the experiment the flow rate was precisely measured every hour for each mesocosm and inlet-outlet chemistry was determined. Temperature and salinity were measured with a YSI Brand Model 30 salinity–conductivity–temperature meter (±0.1 °C; ±0.1 ppt). Dissolved oxygen (DO) was measured with a YSI Brand Model 57 Dissolved Oxygen Meter (±0.2 mg l−1), and pHNBS with an Accumet AP72 pH/mV/temperature meter verified spectrophotometrically using m-cresol purple dye according to SOP 7 (Dickson, Sabine & Christian, 2007). AT was measured using a Titrino Model 877 titrator system. Alkalinity samples were equilibrated to 25 °C and run within an hour of being taken. Accuracy and precision of the titrations was confirmed with certified reference materials (CRM Batch 129) from the Dickson Laboratory, Scripps Institution of Oceanography which verified that our measurements of AT were accurate to within 0.18% of the Dickson CRM value. All carbonate parameters were calculated using the program CO2SYS (Pierrot, Lewis & Wallace, 2006) and stoichiometric dissociation constants defined by Mehrbach et al. (1973) and refit by Dickson & Millero (1987).

The mesocosms are well mixed systems and can be represented by a simple box model Andersson et al. (2009). Changes in total alkalinity (AT) are attributed to calcification or carbonate dissolution Murillo, Jokiel & Atkinson (2014). The net calcification (Gnet) can be easily calculated from Eq. (9) by measuring the amount of material in the inflowing (Fin) and outflowing (Fout) seawater, and the change per unit time in the mesocosm seawater between consecutive sampling times. For Gnet the resulting value is divided by 2 because two moles of AT are produced for every mole of CaCO3 precipitated (calcification) or removed (dissolution) as shown by Eqs. (3)(5). Gnet=FinATFoutATdATdt2. Pnet was measured in a similar manner using O2 concentration, with one mole of carbon being produced for every mole of O2 produced as shown by Eqs. (6)(8). Likewise DIC and H+ were calculated using Eqs. (11) and (12). Pnet=FinO2FoutO2dO2dt DICnet=FinDICFoutDICdDICdt Hnet+=FinH+FoutH+dH+dt.

Results and Discussion

All of the measurements taken during this experiment are shown in Table 2.

Table 2:
Measurements made during the mesocosm experiment of April 24–25, 2012.
Time Irradiance
µ mole
m−2 h−1
Inlet—all mesocosms Outlet Algae only mesocosm
pH AT Temp
O2 In
mg l−1
Flow liters
pH AT Temp
O2 Out
mg l−1
G net P net Mean
6:00 0 34.8 7.95 2196.5 23.1 6.0 7.50 7.93 2196.0 23.0 6.0
7:00 56 34.9 7.95 2198.3 23.5 6.0 7.50 7.93 2196.7 23.2 6.1 0.3 22 2.49
8:00 222 34.8 8.03 2199.0 23.5 6.0 7.50 8.01 2193.5 23.3 6.4 1.0 127 2.70
9:00 464 34.9 8.03 2185.0 23.5 6.3 7.50 8.02 2190.7 23.4 7.1 0.0 340 2.93
10:00 854 34.8 8.06 2200.3 23.3 6.9 7.33 8.06 2182.9 23.6 8.0 1.6 539 3.09
11:00 1619 34.8 8.06 2206.2 23.9 6.6 7.50 8.11 2198.5 23.6 8.2 3.4 746 3.41
12:00 1705 34.8 8.09 2197.7 23.8 6.7 7.67 8.14 2199.6 24.4 7.8 0.8 756 3.70
13:00 1468 34.8 8.09 2200.1 24.0 6.6 7.50 8.16 2195.7 24.4 7.5 0.3 546 3.86
14:00 1702 34.8 8.10 2202.2 24.0 6.7 7.67 8.16 2194.7 24.6 7.8 1.6 534 3.93
15:00 1001 34.9 8.08 2194.6 24.1 6.7 7.83 8.15 2196.6 24.2 7.6 0.7 504 3.89
16:00 739 34.9 8.09 2208.4 24.1 6.6 7.67 8.15 2199.3 24.1 7.5 1.0 488 3.83
17:00 429 34.9 8.08 2208.1 24.0 6.4 7.67 8.12 2209.3 23.9 6.9 1.1 379 3.72
18:00 159 34.8 8.08 2210.7 23.9 6.3 7.67 8.08 2211.4 23.9 6.3 −0.3 127 3.49
19:00 32 34.9 8.07 2199.0 23.9 6.3 7.50 8.08 2203.3 23.5 6.2 −0.7 −50 3.34
20:00 0 34.9 8.07 2184.7 23.8 6.3 7.67 8.07 2189.4 23.5 6.0 −1.2 −135 3.28
21:00 0 34.9 8.07 2206.4 23.8 6.3 7.67 8.05 2203.0 23.5 6.0 −0.2 −179 3.18
22:00 0 34.9 8.04 2180.8 23.5 6.1 7.67 8.04 2199.1 23.3 6.0 −2.1 −147 3.10
23:00 0 34.9 8.01 2192.5 23.4 6.1 7.67 8.03 2199.4 23.3 5.9 −3.5 −87 3.05
0:00 0 34.9 8.06 2201.4 23.6 6.3 7.67 8.02 2199.2 23.3 6.0 −0.6 −124 2.99
1:00 0 35.0 8.04 2201.4 23.4 6.4 7.67 8.04 2201.2 23.2 5.8 0.3 −252 3.02
2:00 0 34.9 8.09 2214.8 23.7 6.3 7.67 8.06 2207.7 23.3 5.6 1.0 −344 3.13
3:00 0 34.9 8.06 2214.3 23.6 6.1 7.50 8.05 2207.0 23.1 5.8 2.0 −280 3.16
4:00 0 34.9 8.02 2209.2 23.3 6.2 7.50 8.04 2209.3 23.1 5.9 1.0 −169 3.10
5:00 0 34.9 8.10 2216.6 23.6 6.3 7.50 8.06 2211.6 23.4 5.8 0.7 −212 3.14
6:00 0 34.9 8.09 2214.3 23.5 6.1 7.50 8.07 2209.6 23.3 5.8 1.3 −216 3.23
Time Outlet coral plus Algae mesocosm Outlet coral only mesocosm
Flow liters
pH AT Temp
O2 Out
mg l−1
G net P net Mean
Flow liters
pH AT Temp
O2 Out
mg l−1
G net P net Mean
6:00 7.50 7.89 2190.8 23.0 5.6 8.33 7.93 2181.6 23.0 5.9
7:00 7.50 7.92 2179.7 23.1 5.8 3.3 −264 2.36 8.33 7.89 2179.1 23.1 6.0 4.6 −59 2.38
8:00 7.50 7.97 2174.0 23.3 6.3 6.1 −67 2.55 8.00 7.96 2171.9 23.2 6.3 6.5 65 2.45
9:00 7.33 8.03 2165.2 23.4 7.5 6.2 361 2.83 8.17 7.99 2170.1 23.3 7.2 5.8 327 2.69
10:00 7.50 8.08 2156.9 23.5 8.9 8.5 883 3.12 8.33 8.04 2154.7 23.8 8.0 8.1 553 2.92
11:00 8.17 8.14 2165.3 24.3 8.4 11.6 956 3.49 8.17 8.10 2167.7 24.3 7.8 11.5 650 3.27
12:00 7.33 8.16 2165.7 24.5 8.4 10.2 983 3.80 8.00 8.12 2162.6 24.5 7.9 10.3 685 3.55
13:00 7.67 8.17 2162.9 24.4 8.1 9.3 853 3.89 8.33 8.13 2157.9 24.4 7.5 10.4 582 3.64
14:00 7.67 8.17 2159.3 24.6 8.4 10.8 845 3.93 8.33 8.12 2159.0 24.6 7.7 11.5 521 3.64
15:00 8.00 8.16 2164.4 24.3 8.1 9.5 768 3.89 8.67 8.10 2158.6 24.3 7.5 10.2 466 3.54
16:00 7.83 8.14 2174.3 24.0 7.8 9.0 644 3.77 8.00 8.09 2169.1 24.0 7.5 10.5 477 3.43
17:00 7.50 8.11 2183.0 23.9 7.0 8.3 472 3.61 8.00 8.09 2176.9 23.9 6.7 9.9 347 3.39
18:00 7.33 8.08 2194.5 23.6 6.2 5.6 61 3.43 8.33 8.06 2190.2 23.6 6.3 6.9 71 3.30
19:00 7.33 8.04 2190.3 23.6 5.9 3.4 −277 3.21 8.17 8.05 2187.2 23.5 6.0 4.4 −123 3.17
20:00 7.33 8.03 2172.5 23.2 5.9 2.9 −366 3.04 8.17 8.04 2177.7 23.3 6.0 2.6 −183 3.09
21:00 7.33 8.03 2192.6 23.2 5.6 3.6 −450 2.99 8.17 8.04 2192.5 23.2 5.8 2.9 −247 3.05
22:00 7.50 8.03 2189.4 23.2 5.6 0.7 −484 3.00 7.83 8.03 2185.6 23.3 5.7 1.3 −292 3.03
23:00 7.50 8.01 2190.4 23.1 5.6 −0.9 −410 2.94 8.17 8.02 2189.5 23.2 5.7 −0.2 −221 2.98
0:00 7.67 7.99 2188.3 23.2 5.6 2.0 −446 2.84 8.33 8.00 2188.6 23.2 5.8 2.1 −242 2.89
1:00 7.33 8.01 2190.2 23.2 5.4 3.3 −621 2.84 8.17 8.01 2190.2 23.2 5.6 3.3 −373 2.87
2:00 7.67 8.03 2196.5 23.3 5.2 4.0 −691 2.96 8.33 8.03 2194.1 23.2 5.4 4.3 −462 2.95
3:00 7.50 8.03 2197.2 23.2 5.3 4.9 −651 3.02 8.17 8.03 2195.7 23.2 5.6 5.4 −394 3.01
4:00 7.50 8.02 2200.2 23.1 5.4 3.6 −556 2.98 8.17 8.02 2199.3 23.1 5.7 3.9 −297 2.98
5:00 7.50 8.03 2200.5 23.4 5.4 3.4 −578 2.99 8.17 8.05 2199.1 23.2 5.6 3.8 −328 3.04
6:00 7.83 8.02 2200.3 23.3 5.4 4.0 −538 3.00 8.33 8.04 2199.1 23.2 5.7 4.4 −295 3.10
DOI: 10.7717/peerj.378/table-2

Calcification over the 24 h period (Fig. 1) shows the diurnal pattern related to irradiance, light enhanced calcification and dark calcification. Values for Gnet are high due to the large biomass of live coral, high solar irradiance in the shallow mesocosms and absence of sediment or dead carbonate skeleton which are subject to dissolution. Gnet in the “Corals only” and “Corals plus Algae” treatments track each other closely. Light saturation of calcification did not occur up to the maximum irradiance which exceeded 1,500 µmole photons m−2 s−1. This value is many times higher than that supplied by the artificial light typically used is most laboratory studies of coral calcification. Calcification rate is very low in the “Algae only” treatment due to low biomass of calcifying organisms, which are made up of various calcifying epiphytes. Low-levels of dark calcification occur at night. There is a drop in calcification to zero around midnight with a dark calcification rate peak at approximately 03:00 h.

Diurnal net calcification rate (Gnet) and irradiance for the three mesocosms.

Figure 1: Diurnal net calcification rate (Gnet) and irradiance for the three mesocosms.

The relationship between Gnet and Ωarag

The linear regression of Gnet plotted as a function of Ωarag (Fig. 2) has become a widespread method of describing coral and coral reef calcification. A significant statistical relationship is obtained, with substantial variance that is generally assumed to be largely sampling error, or the result of other factors which influence Gnet. However, the explanation appears be more complex, as will be discussed in the following sections.

Net calcification rate (Gnet) plotted as a function of Ωarag for (A) “Coral only” mesocosm, (B) “Coral and Algae” mesocosm and (C) “Algae only” mesocosm.

Figure 2: Net calcification rate (Gnet) plotted as a function of Ωarag for (A) “Coral only” mesocosm, (B) “Coral and Algae” mesocosm and (C) “Algae only” mesocosm.

Net calcification rate versus Ωarag.

Figure 3: Net calcification rate versus Ωarag.

Net calcification rate versus Ωarag with each point labeled with hour of the day revealing the clockwise coral reef diel hysteresis pattern for: (A) “Coral only” mesocosm, (B) “Coral plus Algae” mesocosm and the (C) “Algae only” mesocosm, which showed no pattern.

Diel hysteresis, phase lags and night calcification patterns

McMahon et al. (2013) quantified Gnet in a healthy coral reef lagoon in the Great Barrier Reef during different times of day. Their observations revealed a diel hysteresis pattern in the Gnet versus Ωarag relationship. This phenomenon can be demonstrated by labeling the points in Fig. 2 with the hour of day as shown in Fig. 3. The diel pattern moves from the lower left quadrant early in the day toward the upper right through mid-day and then back to the lower center during the night before returning to the lower left quadrant at first light. The pattern is nearly identical for the “Corals only” mesocosm (Fig. 3A) and the “Corals plus Algae” (Fig. 3B), which tracked each other closely (Fig. 1). The “Algae only” mesocosm did not show this pattern. The linear regression for the Gnet vs. Ωarag data for the mesocosm with coral (Fig. 2) accounted for part of the variance (R2 = 0.40). A linear regression does not adequately describe the variance resulting from the diel pattern.

Cyronak et al. (2013) used chambers to measure in situ benthic solute fluxes at three different advection rates at Heron Island lagoon, Australia and observed a strong diurnal hysteresis pattern similar to that in Fig. 3. They suggested that diel hysteresis is caused by the diurnal interaction between photosynthesis and respiration. The data did not follow a trend consistent with the Ωarag of the water column being the main driver of carbonate precipitation and dissolution. Instead, carbonate precipitation and dissolution in these sediment communities is linearly correlated to the rates of photosynthesis and respiration (Pnet) occurring over the same time period.

Phase shifts

Evaluation of phase relations for the various parameters listed in Table 2 can be facilitated by scaling each variable on a 0 to 1 scale. The normalized value of ai for variable A in the ith row was calculated using the equation: Normalized value ai=aiAminAmaxAmin where Amin is the minimum value for variable A and Amax is the maximum value for variable. Figure 4 summarizes the results for the variables most often considered in the literature (pH, Ωarag, Pnet and Gnet).

Figure 4 shows that peak pH and Ωarag lag behind Gnet throughout the daily cycle by two or more hours. The figure also shows that peak Gnet follows Pnet during daylight photosynthetic hours with a reverse during the nighttime hours. Shamberger et al. (2011) reported that Ωarag lags behind Gnet on the reefs of Kaneohe Bay, Hawaii. McMahon et al. (2013) reported that peak Gnet rates occurred 2–3 h before the Ωarag maximum on a healthy coral reef on the Great Barrier Reef. Thus Ωarag (along with closely correlated [CO32−], pH and [DIC]:[H+] ratio) is not the primary driver of coral calcification over a diurnal cycle. The paradigm that Ωarag correlates with Gnet on a global scale must be tempered with the caveat that other processes have a much greater influence on calcification on smaller spatial and temporal scales. The data presented above show that diurnal irradiance drives Pnet, which in turn drives Gnet, and which alters pH, which controls [CO32−] and Ωarag as well as other variables based on concentration such as the ratio of [DIC] to [H+]. A better understanding of this hierarchy will resolve many of the contradictions in the literature on coral reef calcification.

Normalized pH, Ωarag, Pnet and Gnet values for the three mesocosms versus time of day using data from Table 2 and Eq. (9).

Figure 4: Normalized pH, Ωarag, Pnet and Gnet values for the three mesocosms versus time of day using data from Table 2 and Eq. (9).

Arrows point to relative maxima for each parameter.

Night calcification

Laboratory studies show that coral calcification continues in darkness, but at a lower rate than observed in light enhanced calcification (Schneider & Erez, 2006). Night calcification rates have generally been assumed to be low and constant at night, although this assumption has largely gone untested. Figures 1 and 4 show decreasing dark calcification following sunset, reaching zero near midnight followed by an increasing rate of dark calcification and an increase in respiration (Figs. 5C and 5D) that rises to a peak at 03:00 well before dawn. This pattern has occurred consistently in our mesocosm experiments, with the same pattern observed in 30 separate mesocosm runs with different communities under various conditions as well as in flume studies at our site (Murillo, Jokiel & Atkinson, 2014). Barnes & Crossland (1980) used time-lapse photography to measure diurnal growth in the staghorn coral Acropora acuminata and found that night-time extension rate was similar to or greater than day-time extension. They suggested that, “symbiotic association permits rapid growth because the coral can invest in flimsy scaffolding at night with the certainty that bricks and mortar will be available in the morning”. Wooldridge (2013) has proposed a new model for “dark” coral calcification, whereby O2-limitation of aerobic respiration during the night initiates a homeostatic host response that forms the skeletal organic matrix. The matrix formed at night subsequently allows rapid growth of the aragonite fibers during the “light-enhanced” period of calcification, when abundant energy derived from photosynthesis is available. Perhaps the mid-night calcification minimum observed in Figs. 1 and 4 at 00:00 reflects this period of organic matrix formation that precedes the 03:00 night calcification peak.

Diurnal changes in concentration of AT, pH, Ωarg and DO

The variables of AT, pH, Ωarg DIC, and DO are concentrations while Pnet and Gnet are flux rates. Care must be taken when comparing concentrations to flux rates because flux rate can be high when concentration is high or low. Or flux rate can be low when concentration is high or low. Figure 4 shows patterns that are difficult to interpret because the figure mixes flux rates with concentrations. This issue will be discussed and resolved later in this discussion, but first we will compare differences in concentrations of key variables over the diurnal cycle (Fig. 5).

Diurnal changes in seawater chemistry in the three mesocosms for: (A) total alkalinity AT, (B) aragonite saturation state Ωarag, (C) pH and (D) dissolved oxygen.

Figure 5: Diurnal changes in seawater chemistry in the three mesocosms for: (A) total alkalinity AT, (B) aragonite saturation state Ωarag, (C) pH and (D) dissolved oxygen.

Figure 5 reveals several important patterns:

  1. Alkalinity in the “Algae only” mesocosm remained high during the entire diurnal cycle. In contrast, the mesocosms containing corals showed lower AT (Fig. 5A) caused by rapid calcification. AT reduction by the corals was greatest during the daylight hours when Gnet was high (Fig. 1) with the difference diminishing during nighttime hours.

  2. The two mesocosms with algae maintained a higher Ωarag throughout the mid-day portion of the diurnal cycle (Fig. 5B) which can be attributed to higher pH resulting from rapid rates of algae photosynthesis and coral photosynthesis (Eqs. (6)(8)), with a less pronounced difference during the rest of the cycle.

  3. The extreme difference in Ωarag between the “Corals only” and the “Corals plus Algae” mesocosms (Fig. 5B) did not produce a corresponding difference in Gnet between the two mesocosms (Fig. 1), which demonstrates that Ωarag is uncoupled from Gnet and explains differences encountered when comparing the Ωarag versus Gnet relationship in different systems with different diurnal Pnet regimes.

  4. Night-time pH and Ωarag values (Figs. 5B and 5C) show less variability than Gnet (Fig. 1).

  5. The high biomass in the “Coral plus Algae” mesocosm (Fig. 5D) resulted in the highest O2 values during daylight hours (due to photosynthesis) and the lowest O2 during the night (due to respiration). The “Algae only” treatment had the second highest daytime level O2 due to algal photosynthesis and relatively high levels of O2 at night.

  6. The 03:00 calcification peak observed in Fig. 1 is shown by both a decrease in O2 concentration and a drop in pH due to accelerated respiration. DO (Fig. 5D) and the pH (Fig. 5C) are measured independently and both show this effect to corroborate the observation.

Hourly DIC versus AT for the diurnal data measured in each of the three mesocosms.

Figure 6: Hourly DIC versus AT for the diurnal data measured in each of the three mesocosms.

Successive hours are connected by the dotted lines to show the patterns of diurnal hysteresis.

Plotting DIC versus AT (Fig. 6) demonstrates the major influence of Pnet on seawater Ωarag. Calcification and dissolution shift AT values horizontally along the abscissa in Fig. 6 and influence DIC values vertically along the ordinate. However, photosynthesis and respiration change DIC along the ordinate without changing AT. The observed hysteresis pattern results from Pnet driving Gnet and increasing pH. A linear relationship accounting for only half of the variance (R2 ≈ 0.5) between DIC and AT was observed for the two rapidly calcifying mesocosms containing corals. This relationship does not hold for the low-calcification “Algae only” mesocosm.

As pointed out by McMahon et al. (2013), connecting the points on a graph of AT vs. DIC reveals a circular hysteresis pattern over the diel cycle as shown for the Gnet versus Ωarag plot (Fig. 6). Gnet can account for changes in both the AT and DIC concentrations. However, Pnet can only account for changes DIC concentration. Therefore, Ωarag is a function of the changes in carbonate chemistry due to both Pnet and Gnet, and any changes in DIC concentration relative to AT will result in different influences on Ωarag. For example, in systems with high organic production relative to calcification (Coral plus Algae mesocosm), Ωarag will increase during daylight due to high pH caused by high uptake of CO2 used for photosynthesis (Fig. 5D). Conversely, in systems with low organic production relative to calcification (Coral only mesocosm), Ωarag will decrease due to the uptake of AT. Any decrease in Gnet associated with an increase in Pnet will increase Ωarag and change the way that Gnet responds to OA. Therefore, any prediction of future global changes on coral reef Gnet based on oceanic seawater Ωarag must also take into account the influence of future localized Pnet on Gnet and Ωarag as well as changes in carbonate dissolution of reef carbonates as described by Murillo, Jokiel & Atkinson (2014) for each reef location.

Comparisons between the hourly and daily Gnet and Pnet values (Table 3) show a similar calcification rate for both the “Coral only” mesocosm and the “Coral plus Algae” mesocosm in spite of the differences in DO, pH, AT (Fig. 5) and Pnet. However, daily Pnet for the “Coral plus Algae” mesocosm was only one third of the Pnet of the “Coral only” mesocosm. Hourly production was much higher in the “Corals plus Algae” mesocosm during the daylight hours, but production was consumed by extremely high respiration during nighttime hours. The “Algae only” mesocosm showed very low daily Gnet and extremely high daily Pnet.

Table 3:
Hourly and daily Gnet and Pnet values for the three mesocosms.
Solar irradiance Gnet (mmol m−2 h−1) Pnet (mmol m−2 h−1)
Time of day µmol photons m−2 s−1 Corals only Corals plus Algae Algae only Corals only Corals plus Algae Algae only
07:00 56.3 4.6 3.3 0.3 −59 −264 22
08:00 221.6 6.5 6.1 1.0 65 −67 127
09:00 464.6 5.8 6.2 0.0 327 361 340
10:00 854.0 8.1 8.5 1.6 553 883 539
11:00 1619.0 11.5 11.6 3.4 650 956 746
12:00 1705.0 10.3 10.2 0.8 685 983 756
13:00 1468.0 10.4 9.3 0.3 582 853 546
14:00 1702.0 11.5 10.8 1.6 521 845 534
15:00 1001.0 10.2 9.5 0.7 466 768 504
16:00 739.0 10.5 9.0 1.0 477 644 488
17:00 429.0 9.9 8.3 1.1 347 472 379
18:00 159.0 6.9 5.6 −0.3 71 61 127
19:00 31.7 4.4 3.4 −0.7 −123 −277 −50
20:00 0.0 2.6 2.9 −1.2 −183 −366 −135
21:00 0.0 2.9 3.6 −0.2 −247 −450 −179
22:00 0.0 1.3 0.7 −2.1 −292 −484 −147
23:00 0.0 −0.2 −0.9 −3.5 −221 −410 −87
24:00 0.0 2.1 2.0 −0.6 −242 −446 −124
01:00 0.0 3.3 3.3 0.3 −373 −621 −252
02:00 0.0 4.3 4.0 1.0 −462 −691 −344
03:00 0.0 5.4 4.9 2.0 −394 −651 −280
04:00 0.0 3.9 3.6 1.0 −297 −556 −169
05:00 0.0 3.8 3.4 0.7 −328 −578 −212
06:00 0.0 4.4 4.0 1.3 −295 −538 −216
Daily (mmolm−2d−1) 144 133 10 1226 427 2913
DOI: 10.7717/peerj.378/table-3

Anthony, Kleypas & Gattuso (2011) proposed a model that areas dominated by algal beds draw CO2 down and elevate Ωarag, potentially offsetting ocean acidification impacts at the local scale. Their model is based on the paradigm that Gnet is controlled by Ωarag. Results suggested that a shift from coral to algal abundance under ocean acidification can lead to improved conditions for calcification (i.g. increased Ωarag) in downstream habitats and that alga beds can provide a significant mechanism for buffering ocean acidification impacts at the scale of habitat to reef. However, this conclusion is at odds with the measured values shown in Table 3 and Fig. 5. Gnet in the “Corals plus Algae” treatment was the same as the “Coral Only” treatment even though the Ωarag was much higher. In addition, the presence of the algae caused a precipitous drop in Pnet. The flaw in their model appears to be the assumption that Gnet is controlled by Ωarag. Algal photosynthesis increases pH which shifts the equilibrium to higher [CO32−] and thus higher Ωarag. There is a direct correlation between Gnet and Ωarag for a specific reef community, but not a cause and effect relationship.

Diurnal changes in material flux (Pnet, Gnet, H+ flux and DIC flux)

Gnet and Pnet are measures of material flux. DO, pH and DIC are measures of concentration. The preceding discussion and numerous publications often compare concentrations of one material to flux rate of another material or vice versa. Much more can be learned by plotting DIC flux and H+ flux rather than [DIC], [H+] or pH in relation to Pnet and Gnet. DIC flux and H+ flux were calculated using the box model and graphed on a 0 to 1 scale in the same manner as in Fig. 4 with the result presented as Fig. 7. This figure illustrates the dynamic geochemical and physiological relationships involved in coral and coral reef metabolism.

DIC flux (uptake) in the highly calcifying mesocosms containing coral (Fig. 7) increases with increasing Pnet from 06:00 until mid-day peak Pnet and then decreases rapidly as Pnet decreases with decreasing irradiance. Furla et al. (2000) demonstrated the presence of a DIC pool within coral tissues. The size of this pool was dependent on the lighting conditions, since it increased 39-fold after 3 h of illumination. If we apply this observation to the data shown in Fig. 7, it appears that the DIC pool had increased by mid-day, so rate of DIC uptake dropped rapidly as irradiance and photosynthesis declined. However, note that the high dissipation rates of H+ continued for 2–3 h following the peak rates of Pnet and Gnet as the corals rid themselves of the backlog of H+ generated by rapid calcification. Thus the lag of pH behind the peak flux rates of Pnet and Gnet (Figs. 4A and 4B) represents a disequilibrium that results from the lag in proton efflux from the corals. The correlation between Ωarag and Gnet is simply the response of the CO2-carbonate system to pH as [H+] shifts the equilibria and redistributes the [CO32−] relative to the other DIC components of [HCO3] and [CO2] (Eqs. (3)(5)) . Therefore Ωarag closely tracks pH whereas Gnet tracks Pnet more closely. Changes in Ωarag are a consequence of changes in Pnet and Gnet, rather than a driver of Gnet. Hence the Ωarag peak and the pH peak lag behind the Pnet and Gnet peaks (Figs. 4A and 4B) due to lag in proton efflux seen in Fig. 7. This observation demonstrates the importance of understanding the difference between H+ concentration and H+ flux.

During the night the H+ flux rate is very responsive to changes in Gnet in the “Algae only” and “Coral plus Algae” due to large changes in respiration (Fig. 7). The fluctuations of proton flux at night in the “Coral only” mesocosm are dampened considerably compared to the “Algae only” treatment. The “Coral plus Algae” mesocosm shows an intermediate response. Perhaps the coral skeleton acts as a buffer in a manner similar to that proposed by Suzuki, Nakamori & Kayanne (1995). The macroalgae lack the large skeletal carbonate buffer of reef corals.

Plot of normalized data for Pnet, Gnet, inverse DIC flux and H+ flux for the experiment.

Figure 7: Plot of normalized data for Pnet, Gnet, inverse DIC flux and H+ flux for the experiment.

Back to the basics

The preceding sections have established the importance of using flux rates rather than concentrations when we are describing a dynamic metabolic system such as a coral or coral reef. Most of the previous research in this area has focused on the relationship between Gnet, [CO32−] (or its surrogate Ωarag), [HCO3], and [H+] expressed as pH. Plotting these variables in exemplary Fig. 8 is very informative and sheds light on results of previous studies.

A coral must uptake inorganic carbon in order to maintain photosynthesis and calcification. As a result [DIC] will decrease no matter which carbonate species (HCO3, CO32− or CO2) is taken up by the coral (Eqs. (3)(5)). Thus we see a decline in [DIC] at high rates of Gnet (Fig. 8). [HCO3], which has been identified as the preferred substrate for photosynthesis and calcification (Weis, Smith & Muscatine, 1989; Furla et al., 2000; Roleda, Boyd & Hurd, 2012) closely tracks [DIC] during daylight hours. In contrast, [CO32−] lags behind Gnet and closely tracks pH during the day as shown for Ωarag in Fig. 4. If [CO32−] (or its surrogate Ωarag) drives calcification, then how do we explain the lag behind Gnet? And if [CO32−] is limiting, how do we explain the fact that [CO32−] is increasing rather than decreasing as the coral calcifies rapidly and takes up inorganic carbon? [CO32−] increases because of the increase in pH caused by rapid photosynthesis, which shifts the equilibrium between [HCO3] and [CO32−]. Thus, Pnet is the driver of changes in Gnet and [CO32−] (Eqs. (2)(5)). A basic physiological interpretation of the patterns shown in Fig. 8 is that daytime coral metabolism rapidly removes DIC (primarily in the form of HCO3) while photosynthesis provides the energy that drives Gnet (Fig. 4). Higher pH resulting from rapid photosynthesis pushes the equilibria toward higher [CO32−]. This scenario results in a correlation between Gnet and Ωarag, with Ωarag as the dependent variable.

The flux rate of calcification-dissolution (Gnet) plotted against the concentrations of important variables of the CO2-carbonate system for the “Corals only” mesocosm.

Figure 8: The flux rate of calcification-dissolution (Gnet) plotted against the concentrations of important variables of the CO2-carbonate system for the “Corals only” mesocosm.

During the night [HCO3], [DIC], [CO32−] and pH mirror changes in Gnet. However, note that [HCO3] diverges from [DIC] and [CO32−] diverges from pH in darkness. The night divergence can be attributed to respiration causing a decrease in pH. The decreasing pH shifts the equilibria so that [CO32−] is converted to [HCO3], thereby changing the offset between the points. This phenomenon is also reflected in the pattern of diurnal hysteresis show in Fig. 3.

Conclusions and Recommendations

Correlations do not establish cause and effect

Linear regression using Ωarag as the independent variable may be useful as a first approximation, but is a poor descriptor of calcification dynamics on coral reefs. Much of the existing data on coral calcification was developed in static or low turnover incubation experiments under typical laboratory low irradiance artificial light sources on a 12 h light, 12 h dark cycle (Jokiel, Bahr & Rodgers, in press). This regime results in an unrealistic simulation of the actual diurnal cycle that occurs on coral reefs. The standard protocol has been to compare linear regressions between or among treatments. Linear regression provides a very limited description of the actual relationship between the key factors controlling organic and inorganic processes on coral reefs, which are more adequately described by data presentations such as that in Table 3 or Fig. 7. The linear regression approach does not fully embrace natural diurnal calcification patterns and phase lags because these processes are non-linear. The linear regression approach can lead to the assumption that Ωarag is the independent variable driving the calcification reaction. Nevertheless, correlations at a single location or in a single experiment can result where all other factors are held constant because the two quantities are related to some extent. Use of Ωarag as an independent variable to compare spatial and temporal variation in Gnet is known to create difficulties (Shamberger et al., 2011; Falter et al., 2012).

Numerous field and laboratory studies have demonstrated a positive correlation between Gnet and Ωarag for corals and coral reefs Erez et al. (2011). Well-developed reefs occur within a narrow geographic range characterized by open ocean Ωarag > 3.3 (Kleypas et al., 1999), which could mean that coral communities have limited capacity to adapt to future levels of anthropomorphic ocean acidification (OA) projected for the 21st century. Recent reports suggest that healthy coral reefs could cease to exist within this time frame as OA continues and oceanic Ωarag decreases (Hoegh-Guldberg et al., 2007; Silverman et al., 2009). However, there are inconsistencies in the relationship (slope and x-intercept) between Gnet as a function of Ωarag on various reefs throughout the world (Shamberger et al., 2011). For example, Kaneohe Bay, Oahu, Hawaii contains rich coral reefs that show extremely high rates of Gnet while living at low Ωarag levels (mean Ωarag = 2.85) (Shamberger et al., 2011). Shamberger et al. (2014) report the existence of highly diverse, coral-dominated reef communities at the Rock Islands of Palau that are living at low saturation states (Ωarag = 1.9–2.5). These values approach those projected for the tropical western Pacific open ocean by 2100 under future OA modeling scenarios. Identification of biological and environmental factors that enable these communities to persist at low Ωarag could provide important insights into the future of coral reefs under increasing OA. So how do we account for the paradox of rich coral reefs growing at low Ωarag? Previous work has been based on the assumption that Gnet is controlled by or related directly to Ωarag. The present investigation indicates that Pnet rather than Ωarag drives Gnet and that calcification rate is further limited by proton flux, with pH and AT playing the major role in controlling calcification. Ωarag on coral reefs is simply a dependent variable being controlled largely by changes in pH due to photosynthesis. A correlation will exist at a given site, but will not be consistent between different coral reef communities.

The [DIC]:[H+] ratio correlates with Ωarag in describing Gnet and is useful from a physiological point of view because it involves pH and all of the inorganic carbon species (Jokiel, 2011a; Jokiel, 2013). However, the [DIC]:[H+] ratio is simply another variable based on concentration (along with pH, Ωarag, CO32−, etc.) that shows a correlation with Gnet. Nevertheless, the [DIC]:[H+] ratio can be important in describing Gnet in situations where Ωarag is decoupled from [H+] as occurs in the paleo-ocean over time scales greater than 10,000 years (Hönisch et al., 2012). A calcifying organism must uptake DIC in order to continue the calcification reaction and must rid itself of the waste protons. So Gnet correlates directly to [DIC] and inversely to [H+].

Results of this investigation (Fig. 7) demonstrate the difficulty that corals encounter in shedding waste protons generated during calcification. High rates of H+flux continued for several hours following peak Gnet. An important conclusion of this work is that measurements of DIC flux and H+ flux are far more useful in describing coral metabolism dynamics than [DIC] and [H+] (Fig. 8). Likewise, Ωarag is not a very useful variable in that it simply tracks pH (Fig. 4). This pattern becomes clear when one considers that [CO32−] (and hence Ωarag) shifts with changing [H+] as described in Eqs. (2)(5). DIC flux follows Pnet and Gnet and decreases rapidly following peak Pnet and peak Gnet indicating that corals can cope more effectively with the problem of DIC supply compared to the problem of eliminating H+.

Future research directions

The time lag between Gnet and Ωarag reported previously in field studies (Shamberger et al., 2011; Cyronak et al., 2013; McMahon et al., 2013) provides evidence that diffusion and advection of materials between the coral and the water column involves time delays. One reason is that corals convert inorganic carbon to organic carbon, translocate the organic carbon to distal calcification sites, store organic carbon as lipid, and can eventually convert stored organic carbon back to inorganic carbon (Jokiel, 2011b), creating numerous possible phase lags for metabolic materials. The second reason for the time lag is that rapidly calcifying systems have difficulty dissipating waste protons as shown by continued rapid proton efflux for hours after peak calcification (Fig. 7). What other mechanisms can account for the phase lag? Boundary layers (BL) can slow the exchange of metabolic materials between the coral and the water column. The results of Cyronak et al. (2013) revealed that stirring had a net stimulatory effect on AT flux and on the diurnal cycle of hysteresis. Boundary layers slow exchange of metabolic materials, so this is an area of investigation that can provide an explanation.

Three hydrodynamic boundary layers have previously been defined and measured (Shashar, Cohen & Loya, 1993; Shashar et al., 1996). The Diffusion Boundary Layer (DBL) is only a few mm thick and in contact with the coral epidermis. The Momentum Boundary Layer (MBL) controls water movement in the proximity of the sessile organisms and is thicker by an order of magnitude than the DBL. The Benthic Boundary Layer (BBL), which controls the interactions of the reef with the surrounding sea water, was typically found to be more than 1 m thick and characterized by a roughness height of 31 cm and a shear velocity of 0.42 cm s−1 in the studies.

The DBL is a thin layer of stagnant seawater adjacent to the coral produced by frictional drag. This quiescent layer influences the flux of material between the benthic surface and the water column. The transport of Ca2+, CO2, CO32−, HCO3, O2, nutrients and H+ through the DBL is limited by the physical processes of diffusion and advection (Jokiel, 1978; Lesser et al., 1994; Kaandorp et al., 2005; Kaandorp, Filatov & Chindapol, 2011). Kühl et al. (1995) found that zooxanthellae photosynthesis resulted in a build-up of O2 in the photosynthetic tissue of up to 250% saturation and a tissue pH of up to 8.6 (i.e., 0.7 pH units above the pH value of the overlying seawater). In darkness the O2 within the coral tissue was depleted by respiration to near anoxic (<2% air saturation) conditions, with tissue pH of 7.3–7.4. O2 and pH profiles demonstrated the presence of a 200–300 µm thick DBL that separated the coral tissue from the overlying flowing seawater. Various models invoke boundary layer controls on coral metabolism. Kaandorp et al. (2005) and Kaandorp, Filatov & Chindapol (2011) addressed DBL limitation of DIC influx while Jokiel (2011a), Jokiel (2011b) and Jokiel (2013) challenged the paradigm that calcification is limited by CO32− supply on the reactant side of the calcification equation. Rather, he argued that rate of dissipation of H+ on the product side due to boundary layer conditions can be the actual limiting factor.

Boundary layer limitation of photosynthesis provides an analog to boundary layer limitation of calcification. Photosynthetic rate can be limited by rate of waste O2 dissipation through the boundary layer rather than being limited by supply of reactant CO2. By analogy, calcification can be limited by rate of removal of waste protons rather than by availability of inorganic carbon. The importance of water motion in reducing boundary layer thickness and thereby increasing oxygen flux between the photosynthetic organisms and the water column has been demonstrated (Mass et al., 2010). By analogy, increased water motion can decrease boundary layer thickness and thereby increase removal of protons from the coral.

Studies of reef metabolism beginning with the classic work of Odum & Odum (1955) at Enewetak Reef flat and followed by others (Shamberger et al., 2011; Falter et al., 2012) were conducted in shallow water reef flats within the BBL in situations where unidirectional currents allowed calculation of flux rates. Substantial boundary layers occur over all reefs. For example, Price et al. (2012) investigated a range of sites from exposed coastal situations to lagoons and found that ambient variability in pH was substantial and oscillated over a diurnal cycle with diel fluctuations in pH exceeding 0.2. Daily pH maxima were identified as an important control on calcification. Net accretion among sites was positively related to the magnitude and duration of pH above the climatological seasonal low, despite myriad other ecological (e.g., local supply, species interactions, etc.) and physical oceanographic (e.g., temperature, current magnitude and direction, wave strength, latitudinal gradients, etc.) drivers. In general, accretion rates were higher at sites that experienced a greater number of hours at high pH values each day. Where daily pH within the BBL failed to exceed pelagic climatological seasonal lows, net accretion was slower and fleshy, non-calcifying benthic organisms dominated space. Thus, key aspects of coral reef ecosystem structure and function are clearly related to natural diurnal variability in pH, which is driven primarily by photosynthesis and respiration as Pnet.

The master variables

The practice of calculating and comparing linear regressions of Gnet vs. Ωarag to obtain a first approximation of calcification rates under different conditions is fraught with problems but probably will continue because it is ingrained in science and is convenient to use. The correlation of a primary biological response (Gnet) to a primary physical chemistry measurement (Ωarag) is attractive, especially in modeling the possible future changes on coral reefs. Unfortunately, the physical chemistry concept of Ωarag has no basic physiological meaning in describing Gnet other than a correlation with the [DIC]: [H+] ratio (Jokiel, 2013) as well as with other factors such as pH. There is no consistent relationship between Ωarag and Gnet when comparing reefs throughout the world (Shamberger et al., 2011). Coral reefs are systems in constant disequilibrium with the water column. So we must take care not to be led astray in our thinking about the variables that actually drive and control coral and coral reef metabolism and bulk water chemistry. The correlation between Gnet and other factors is a result of Pnet driving both Gnet and Ωarag (McMahon et al., 2013). The observed phenomenon of diurnal hysteresis and diurnal phase lag show the importance of measuring flux rates and emphasizes the challenge in predicting the future effects of OA on coral reefs. The method of using linear extrapolations of Ωarag to determine threshold levels that will shift coral reefs from net calcifying systems to a net dissolving state has been questioned (McMahon et al., 2013). Perhaps predicted changes in Ωarag in the open ocean can be used to calculate changes on reefs if we assume that the baseline on the reefs will change in concert with ocean values and that all other processes such as Pnet and carbonate dissolution will not be influenced by OA. An explanation for the many paradoxes of coral calcification discussed herein has been presented as the “Two Compartment Proton Flux Model of Coral Metabolism” (Jokiel, 2011b). This model is focused on localized gradients that influence coral metabolism with a focus on proton flux, carbon pools and translocation of fixed carbon. A major feature of the model is the presence of boundary layers which control local pH gradients and inorganic carbon speciation in addition to proton flux. Results of the present investigation support this model.