Effect of elevated p CO 2 on trace gas production during an ocean acidification mesocosm experiment

A mesocosm experiment was conducted in Wuyuan Bay (Xiamen), China, to investigate the effects of elevated pCO2 on the phytoplankton species Phaeodactylum tricornutum (P. tricornutum), Thalassiosira weissflogii (T. weissflogii) and Emiliania huxleyi (E. huxleyi) and their production ability of dimethylsulfide (DMS), dimethylsulfoniopropionate (DMSP), as well as four halocarbon compounds, bromodichloromethane (CHBrCl2), methyl bromide (CH3Br), dibromomethane (CH2Br2) and iodomethane (CH3I). Over a period of 5 weeks, P. tricornuntum outcompeted T. weissflogii and E. huxleyi, comprising more than 99 % of the final biomass. During the logarithmic growth phase (phase I), mean DMS concentration in high pCO2 mesocosms (1000 μatm) was 28 % lower than that in low pCO2 mesocosms (400 μatm). Elevated pCO2 led to a delay in DMSP-consuming bacteria concentrations attached to T. weissflogii and P. tricornutum and finally resulted in the delay of DMS concentration in the high pCO2 treatment. Unlike DMS, the elevated pCO2 did not affect DMSP production ability of T. weissflogii or P. tricornuntum throughout the 5-week culture. A positive relationship was detected between CH3I and T. weissflogii and P. tricornuntum during the experiment, and there was a 40 % reduction in mean CH3I concentration in the high pCO2 mesocosms. CHBrCl2, CH3Br, and CH2Br2 concentrations did not increase with elevated chlorophyll a (Chl a) concentrations compared with DMS(P) and CH3I, and there were no major peaks both in the high pCO2 or low pCO2 mesocosms. In addition, no effect of elevated pCO2 was identified for any of the three bromocarbons.


Introduction
Anthropogenic emissions have increased the fugacity of atmospheric carbon dioxide (pCO 2 ) from the pre-industrial value of 280 µatm to the present-day value of over 400 µatm, and these values will further increase to 800-1000 µatm by the end of this century (Gattuso et al., 2015).The dissolution of this excess CO 2 into the surface of the ocean directly affects the carbonate system and has lowered the pH by 0.1 units, from 8.21 to 8.10 over the last 250 years.Further decreases of 0.3-0.4pH units are predicted by the end of this century (Doney et al., 2009;Orr et al., 2005;Gattuso et al., 2015), which is commonly referred to as ocean acidification.The physiological and ecological aspects of the phytoplankton response to this changing environment can potentially alter marine phytoplankton community composition, community biomass, and feedback to biogeochemical cycles (Boyd and Doney, 2002).These changes simultane-Published by Copernicus Publications on behalf of the European Geosciences Union.
ously have an impact on some volatile organic compounds produced by marine phytoplankton (Liss et al., 2014;Liu et al., 2017), including the climatically important trace gas dimethylsulfide (DMS) and a number of volatile halocarbon compounds.
DMS is the most important volatile sulfur compound produced from dimethylsulfoniopropionate (DMSP), which is ubiquitous in marine environments, mainly synthesized by marine microalgae (Stefels et al., 2007), a few angiosperms, some corals (Raina et al., 2016), and several heterotrophic bacteria (Curson et al., 2017) through complex biological interactions in marine ecosystems.Although it remains controversial, DMS and its by-products, such as methanesulfonic acid and non-sea-salt sulfate, are suspected of having a prominent part in climate feedback (Charlson et al., 1987;Quinn and Bates, 2011).The conversion of DMSP to DMS is facilitated by several enzymes, including DMSP lyase and acyl CoA transferase (Kirkwood et al., 2010;Todd et al., 2007); these enzymes are mainly found in phytoplankton, macroalgae, symbiodinium, bacteria and fungi (de Souza and Yoch, 1995;Stefels and Dijkhuizen, 1996;Steinke and Kirst, 1996;Chl a and Yoch, 1998;Yost and Mitchelmore, 2009).Several studies have shown a negative impact of decreasing pH on DMS-production capability (Hopkins et al., 2010;Avgoustidi et al., 2012;Archer et al., 2013;Webb et al., 2016), while others have found either no effect or a positive effect (Vogt et al., 2008;Hopkins and Archer, 2014).Several assumptions have been presented to explain these contrasting results and attributed the pH-induced variation in DMSproduction capability to altered physiology of the algae cells or of bacterial DMSP degradation (Vogt et al., 2008;Hopkins et al., 2010, Avgoustidi et al., 2012;Archer et al., 2013;Hopkins and Archer, 2014;Webb et al., 2015).
Halocarbons also play a significant role in the global climate because they are linked to tropospheric and stratospheric ozone depletion and a synergistic effect of chlorine and bromine species has been reported, accounting for approximately 20 % of the polar stratospheric ozone depletion (Roy et al., 2011).In addition, iodocarbons can release atomic iodine quickly through photolysis in the atmospheric boundary layer and iodine atoms are very efficient in the catalytic removal of O 3 , which governs the lifetime of many climate-relevant gases, including methane and DMS (Jenkins et al., 1991).Compared with DMS, limited attention was received about the effect of ocean acidification on halocarbon concentrations.Hopkins et al. (2010) and Webb et al. (2015) measured lower concentrations of several iodocarbons, while bromocarbons were unaffected by elevated pCO 2 in two acidification experiments.In addition, another mesocosm study did not elicit significant differences from any halocarbon compounds at up to 1400 µatm pCO 2 (Hopkins et al., 2013).
Taken together, the data indicate that the response of DMS and halocarbon release to elevated pCO 2 is complex and controversial.DMS and halocarbons play a significant role in the global climate and will perhaps act to a greater extent in the future.An intermediate step between laboratory and natural community field experiments was designed in this study to understand the response of the release of DMS and halocarbon to ocean acidification in Chinese coastal seas using isolates of non-axenic phytoplankton added to filtered natural water.We hypothesized that the response of DMS and halocarbon release to elevated pCO 2 in natural seawater can be better presented after minimizing the shifting composition of the natural phytoplankton and microbial communities.

Experimental setup
To investigate the response of DMS and halocarbon release to ocean acidification, a mesocosm experiment was carried out on a floating platform (set in seawater, about 150 m from the shore) at the Facility for Ocean Acidification Impacts Study of Xiamen University (FOANIC-XMU; 24.52 • N, 117.18 • E) (for full technical details of the mesocosms, see Liu et al., 2017).Six cylindrical transparent thermoplastic polyurethane bags with domes were deployed along the southern side of the platform.The width and depth of each mesocosm bag were 1.5 and 3 m, respectively.Filtered (0.01 µm ultrafiltration water purifier, MU801-4T, Midea, Guangdong, China) in situ seawater was pumped into the six bags simultaneously within 24 h.A known amount of NaCl solution was added to each bag to calculate the exact volume of seawater in the bags, according to a comparison of the salinity before and after adding salt (Czerny et al., 2013).The initial in situ pCO 2 was about 650 µatm.To set the low (400 µatm) and high pCO 2 (1000 µatm) levels, we added Na 2 CO 3 solution and CO 2 saturated seawater to the mesocosm bags to alter total alkalinity and dissolved inorganic carbon (Gattuso et al., 2010;Riebesell et al., 2013).Subsequently, during the whole experimental process, air at the ambient (400 µatm) and elevated pCO 2 (1000 µatm) concentrations was continuously bubbled into the mesocosm bags using a CO 2 Enricher (CE-100B, Wuhan Ruihua Instrument & Equipment Ltd., Wuhan, China).Seawater taken from the coastal environment was first filtered to remove algae and their attached bacteria before usage in mesocosm bags.Bacterial abundance in the pre-filtered water was less than 10 3 cell mL −1 , which was 3 magnitudes lower than the bacterial abundance in the natural water and close to the detection limit of the flow cytometer.The trace gases, including DMS, bromodichloromethane (CHBrCl 2 ), methyl bromide (CH 3 Br), dibromomethane (CH 2 Br 2 ), and iodomethane (CH 3 I) produced in the environment, did not affect the mesocosm trace gas concentrations after the bags were sealed.

Algal strains
Before being introduced into the mesocosms, the three phytoplankton species Phaeodactylum tricornutum (P.tricornutum), Thalassiosira weissflogii (T.weissflogii) and Emiliania huxleyi (E.huxleyi) were cultured in autoclaved, pre-filtered seawater from Wuyuan Bay at 16 • C (similar to the in situ temperature of Wuyuan Bay) without any addition of nutrients.Cultures were continuously aerated with filtered ambient air containing 400 µatm of CO 2 within plant chambers (HP1000G-D, Wuhan Ruihua Instrument & Equipment, China) at a constant bubbling rate of 300 mL min −1 .The culture medium was renewed every 24 h to maintain the cells of each phytoplankton species in exponential growth.When the experiment began, these three phytoplankton species were inoculated into the mesocosm bags, with an initial diatom/coccolithophorid cell ratio of 1 : 1.The initial concentrations of P. tricornuntum, T. weissflogii, and E. huxleyi inoculated into the mesocosm were 10, 10, and 20 cells mL −1 , respectively.P. tricornuntum and T. weissflogii were obtained from the Center for Collections of Marine Bacteria and Phytoplankton of the State Key Laboratory of Marine Environmental Science (Xiamen University).P. tricornuntum was originally isolated from the South China Sea in 2004 and T. weissflogii was isolated from Daya Bay in the coastal South China Sea.E. huxleyi was originally isolated in 1992 from the field station of the University of Bergen (Raunefjorden; 60 • 18 N, 05 • 15 E).

Sampling for DMS(P) and halocarbons
DMS(P) and halocarbon samples were taken from the abovementioned mesocosm bags at 09:00; then all collected samples were transported into a dark cool box back to the laboratory onshore for analysis within 1 h.For the DMS analysis, a 2 mL sample was gently filtered through a 25 mm GF/F (glass fiber) filter and transferred to a purge and trap system linked to a Shimadzu GC-2014 gas chromatograph (Tokyo, Japan) equipped with a glass column packed with 10 % DEGS on Chromosorb W-AW-DMCS (3 m × 3 mm) and a flame photometric detector (Zhang et al., 2014).For total DMSP analysis, a 10 mL water sample was fixed using 50 µL of 50 % H 2 SO 4 and sealed (Kiene and Slezak, 2006).After > 1-day preservation, DMSP samples were hydrolyzed for 24 h with a pellet of KOH (final pH > 13) to fully convert DMSP to DMS.Then, 2 mL of the hydrolyzed sample was carefully transferred to the purge and trap system mentioned above for extraction of DMS.For halocarbons, a 100 mL sample was purged at 40 • C with pure nitrogen at a flow rate of 100 mL min −1 for 12 min using another purge and trap system coupled to an Agilent 6890 gas chromatograph (Agilent Technologies, Palo Alto, CA, USA) equipped with an electron capture detector (ECD) as well as a 60 m DB-624 capillary column (0.53 mm ID; film thickness, 3 µm) (Yang et al., 2010).The analytical precision for duplicate measurements of DMS(P) and halocarbons was > 10 %.

Measurements of chlorophyll a
Chlorophyll a (Chl a) was measured in water samples (200-1000 mL) collected every 2 days at 09:00 by filtering onto Whatman GF/F filters (25 mm).The filters were placed in 5 mL 100 % methanol overnight at 4 • C and centrifuged at 5000 g for 10 min.The absorbance of the supernatant (2.5 mL) was measured from 250 to 800 nm using a scanning spectrophotometer (DU 800, Beckman Coulter Inc., Brea, CA, USA).Chl a concentration was calculated according to the equation reported by Porra (2002).

Enumeration of DMSP-consuming bacteria
The number of DMSP-consuming bacteria in the mesocosms was estimated using the most probable number methodology.The medium consisted of a mixture (1 : 1 v/v) of sterile artificial seawater and a mineral medium (Visscher et al., 1991), 3 mL of which was dispensed into 6 mL test tubes, which were closed by an over-sized cap, allowing gas exchange.Triplicate dilution series were set up.All test tubes contained 1 mmol L −1 DMSP as the sole organic carbon source and were kept at 30 • C in the dark.After 2 weeks, the presence/absence of bacteria in the tubes was verified by DAPI staining (Porter and Feig, 1980).Three tubes containing 3 mL ASW without substrate were used as controls.

Statistical analysis
One-way analysis of variance (ANOVA), Tukey's test, and the two-sample t test were carried out to demonstrate the differences between treatments.A p value < 0.05 was considered significant.Relationships between DMS(P), halocarbons and a range of other parameters were detected using Pearson's correlation analysis via SPSS 22.0 for Windows (SPSS Inc., Chicago, IL, USA).

Results and discussion
3.1 Temporal changes in pH, Chl a, P. tricornuntum, T.
weissflogii, and E. huxleyi during the experiment During the experiment, the seawater in each mesocosm was well mixed, and the temperature and salinity remained stable, with means of 16 • C and 29, respectively, in all mesocosm bags.We observed significant differences in pH levels between the two CO 2 treatments on days 0-11, but the differences disappeared with subsequent phytoplankton growth (Fig. 1).The phytoplankton growth process was divided into three phases in terms of variations in Chl a concentrations in the mesocosm experiments as described in 3 ) concentrations were 54, 20, 2.6 and 41 µmol L −1 , respectively, for the low pCO 2 treatment and 52, 21, 2.4 and 38 µmol L −1 , respectively, for the high pCO 2 treatment.The nutrient concentrations (NO − 3 , NO − 2 , NH + 4 and phosphate) during phase I were consumed rapidly and their concentrations were below or close to the detection limit during phase II (Table 1).SiO 2− 3 was detectable during the entire experimental period, and was unlikely to be a limiting factor for phytoplankton growth during the experiment.In addition, although dissolved inorganic nitrogen (NH + 4 , NO − 3 , and NO − 2 ) and phosphate were depleted, Chl a concentration in both treatments (biomass dominated by P. tricornuntum) remained constant over days 12-22, and then declined over subsequent days.T. weissflogii was found throughout the entire period in each bag, but the maximum concentration was 8120 cells mL −1 , which was far less than the concentration of P. tricornutum with a maximum density of about 1.5 million cells mL −1 (Liu et al., 2017).It is possible that P. tricornutum outcompeted T. weissflogii because of its higher surface-to-volume ratio and/or species-specific physiology, which would enhance the efficiency of nutrient uptake and related metabolism (Alessandrade et al., 2007).E. huxleyi was only found in phase I and its maximal concentration reached 310 cells mL −1 according to the results of Liu et al. (2017).Previous studies have reported that the maximum specific growth rate of T. weissflogii and P. tricornutum is about 1.2 d −1 (Li et al., 2014;Sugie and Yoshimura, 2016), while that of E. huxleyi is about 0.8 d −1 (Xing et al., 2015).This might be the main reason why diatoms overwhelmingly outcompeted the coccolithophores during this experiment.

Impact of elevated pCO 2 on DMS and DMSP production
DMSP concentrations in the high pCO 2 and low pCO 2 treatments increased significantly along with the increase in Chl a concentrations and algal cells, and remained relatively constant over the following days.A significant positive relationship was observed between DMSP and phytoplankton in the experiment (r = 0.961, p < 0.01 for P. tricornuntum, r = 0.617, p < 0.01 for T. weissflogii in the low pCO 2 treatment, Table 2; r = 0.954, p < 0.01 for P. tricornuntum, r = 0.743, p < 0.01 for T. weissflogii in the high pCO 2 treatment, Table 3).DMS was maintained at a low level during phase I (mean of 1.03 nmol L −1 in the low pCO 2 and 0.74 nmol L −1 in the high pCO 2 treatments, respectively) compared with DMSP.DMS concentrations began to increase rapidly on day 15, peaked on day 25 in the low pCO 2 treatment (112.1 nmol L −1 ) and on day 29 in the high pCO 2 treatment (101.9 nmol L −1 ), respectively, and then decreased in the following days.A moderate positive relationship was observed between DMS and P. tricornuntum (r = 0.560, p < 0.05 in the low pCO 2 treatment; r = 0.635, p < 0.01 in the high pCO 2 treatment), while no relationship was observed be-  tween DMS and T. weissflogii (Tables 2 and 3) during the experiment.Similar to DMS, DMSP-consuming bacteria also maintained a low level during phase I (mean of 0.57 × 10 6 and 0.40 × 10 6 cells mL −1 in the low pCO 2 and high pCO 2 treatments, respectively).DMSP-consuming bacterial concentrations peaked on days 19 (11.65 × 10 6 cells mL −1 ) and 21 (10.70 × 10 6 cells mL −1 ) in the low pCO 2 and high pCO 2 treatments, respectively.In this study, no difference in mean DMSP concentrations was observed between the two treatments, indicating that elevated pCO 2 had no significant influence on DMSP production in P. tricornuntum and T. weissflogii.However, significant reductions in mean DMS concentration (28 %) and DMSP-consuming bacteria (29 %) were detected during phase I in the high pCO 2 treatment compared with those in the low pCO 2 treatment, indicating that elevated pCO 2 inhibited DMSP-consuming bacteria and DMS production during the logarithmic growth phase.In addition, the peak DMS concentration in the high pCO 2 treatment was delayed 4 days relative to that in the low pCO 2 treatment during phase II (Fig. 2a).This result has been observed in previous mesocosm experiments and it was attributed to small-scale shifts in community composition and succession (Vogt et al., 2008;Webb et al., 2016).However, this phenomenon during the present study can be explained in another straightforward way.Previous studies have shown that marine bacteria play a key role in DMS production, and that the efficiency of bacteria converting DMSP to DMS may vary from 2 to 100 % depending on the nutrient status of the bacteria and the quantity of dissolved organic matter (Simó et al., 2002(Simó et al., , 2009;;Kiene et al., 1999Kiene et al., , 2000)).In addition, a significant positive relationship was observed between DMS and DMSP-consuming bacteria (r = 0.643, p < 0.01 in the low pCO 2 treatment; r = 0.544, p < 0.01 in the high pCO 2 treatment) during this experiment.All of these observations point to the importance of bacteria in DMS and DMSP dynamics.During the present mesocosm experiment, DMSP concentrations in the low pCO 2 treatment decreased slightly on day 23, while the slight decrease appeared on day 29 in the high pCO 2 treatment (Fig. 2b).In addition, the time that the DMSP concentration began to decrease was very close to the time when the highest DMS concentration occurred in both treatments.Similar to DMS, DMSP-consuming bacteria were also delayed in the www.biogeosciences.net/15/6649/2018/Biogeosciences, 15, 6649-6658, 2018 high pCO 2 mesocosm compared to those in the low pCO 2 mesocosm (Fig. 2c).Taken together, we inferred that the elevated pCO 2 first delayed growth of DMSP-consuming bacteria; then the delayed DMSP-consuming bacteria postponed the DMSP degradation process, and eventually delayed the DMS concentration in the high pCO 2 treatment.In addition, considering that algae and bacteria in natural seawater were removed through a filtering process before the experiment (Huang et al., 2018), we further concluded that the elevated pCO 2 controlled DMS concentrations mainly by affecting DMSP-consuming bacteria attached to T. weissflogii and P. tricornuntum.

Impact of elevated pCO 2 on halocarbon compounds
The temporal development in CHBrCl 2 , CH 3 Br, and CH 2 Br 2 concentrations is shown in Fig. 3a, b, and c, respectively.The temporal changes in their concentrations were substantially different from those in DMS, DMSP, P. tricornuntum and T. weissflogii.The mean concentrations of CHBrCl 2 , CH 3 Br, and CH 2 Br 2 for the entire experiment were 8.58, 7.85, and 5.13 pmol L −1 in the low pCO 2 treatment and 8.81, 9.73, and 6.27 pmol L −1 in the high pCO 2 treatment.The concentrations of CHBrCl 2 , CH 3 Br, and CH 2 Br 2 did not increase with the Chl a concentration compared with those of DMS and DMSP, and no major peaks were detected in the mesocosms.In addition, no effect of elevated pCO 2 was identified for any of the three bromocarbons, which compared well with previous mesocosm findings (Hopkins et al., 2010(Hopkins et al., , 2013;;Webb et al., 2016).No clear correlation was observed between the three bromocarbons and any of the measured algal groups (Tables 2 and 3), indicating that P. tricornuntum and T. weissflogii did not primarily release these three bromocarbons during the mesocosm experiment.Previous studies reported that large-sized cyanobacteria, such as Aphanizomenon flos-aquae, could produce bromocarbons (Karlsson et al., 2008).Significant correlations between the abundance of cyanobacteria and several bromocarbons have been reported in the Arabian Sea (Roy et al., 2011).However, the filtration procedure led to the loss of cyanobacteria in the mesocosms and finally resulted in low bromocarbon concentrations during the experiment, although P. tricornuntum and T. weissflogii abundances were high.
The temporal dynamics of CH 3 I in the high pCO 2 and low pCO 2 treatments are shown in Fig. 3d.The CH 3 I concentrations in the low pCO 2 treatment varied from 0.38 to 12.61 pmol L −1 , with a mean of 4.76 pmol L −1 .The CH 3 I concentrations in the high pCO 2 treatment ranged between 0.44 and 8.78 pmol L −1 , with a mean of 2.88 pmol L −1 .The maximum CH 3 I concentrations in the high pCO 2 and low pCO 2 treatments were both observed on day 23.The range of CH 3 I concentrations during this experiment was similar to that measured in the mesocosm experiment (< 1-10 pmol L −1 ) in Kongsfjorden conducted by Hopkins et al. (2013).In addition, the mean CH 3 I concentration in the low pCO 2 treatment was similar to that measured in the East China Sea, with an average of 5.34 pmol L −1 in winter and 5.74 pmol L −1 in summer (Yuan et al., 2016).Meanwhile, a positive relationship was detected between CH 3 I and Chl a, P. tricornuntum and T. weissflogii (r = 0.588, p < 0.01 in the low pCO 2 treatment; r = 0.834, p < 0.01 in the low pCO 2 treatment for P. tricornuntum; r = 0.680, p < 0.01 in the low pCO 2 treatment; r = 0.690, p < 0.01 in the high pCO 2 treatment for Thalassiosira weissflogii; r = 0.717, p < 0.01 in the low pCO 2 treatment; r = 0.741, p < 0.01 in the high pCO 2 treatment for Chl a).This result agrees with previous mesocosm (Hopkins et al., 2013) and laboratory experiments (Hughes et al., 2013;Manley and De La Cuesta, 1997) identifying diatoms as significant producers of CH 3 I.Moreover, similar to DMS, the maximum CH 3 I concentration also occurred after the maxima of P. tricornuntum and T. weissflogii, at about 4 days (Fig. 3d).This result was similar to the conclusions reported by Hopkins et al. (2010) and Wingenter et al. (2007) during two mesocosm experiments conducted in Norway.Their results confirmed that iodocarbon gases generally occur after the Chl a maxima.Furthermore, the mean CH 3 I concentration measured in the high pCO 2 treatment was significantly lower (40 %) than that measured in the low pCO 2 treatment during the mesocosm experiment.This result is in accordance with Hopkins et al. (2010) and Webb et al. (2015), who also reported that elevated pCO 2 leads to a reduction in iodocarbon concentrations, but is in contrast to the findings of Hopkins et al. (2013) and Webb et al. (2016), who showed that elevated pCO 2 does not significantly affect the iodocarbon concentrations in the mesocosms.Considering that the phytoplankton species did not show significant differences in the high pCO 2 and low pCO 2 treatments during the experiment, this reduction in the high pCO 2 treatment was likely not caused by phytoplankton.Apart from direct biological production via methyl transferase enzyme activity by both phytoplankton and bacteria (Amachi et al., 2001), CH 3 I is produced from the breakdown of higher molecular weight iodine-containing organic matter (Fenical, 1982) through photochemical reactions between organic matter and light (Richter and Wallace, 2004).Both bacterial methyl transferase enzyme activity and photochemical reaction could be responsible for the reduction of CH 3 I concentrations in the high pCO 2 treatment, but further experiments are needed to verify this result.
In this study, the effects of increased levels of pCO 2 on marine DMS(P) and halocarbon release were studied in a controlled mesocosm facility.During the logarithmic growth phase, the elevated pCO 2 led to a reduction in mean DMSPconsuming bacteria (29 %) and DMS concentration (28 %) compared with those in the low pCO 2 treatment.In addition, a 4-day delay in DMS concentration was observed in the high pCO 2 treatment due to the effect of elevated pCO 2 , and we attribute this delay in DMS concentration to the DMSP-consuming bacteria attached to P. tricornuntum and T. weissflogii.Due to the loss of main bromocarbonproducing species affected by the filtration procedure, three bromocarbon compounds measured in this study were not correlated with P. tricornuntum and T. weissflogii, and Chl a.In addition, elevated pCO 2 had no effect on any of the three bromocarbons.The temporal dynamics of CH 3 I, combined with strong correlations with P. tricornuntum and T. weissflogii, and Chl a, indicate that P. tricornuntum and T. weissflogii play a critical role in controlling CH 3 I concentrations.In addition, the production of CH 3 I was sensitive to pCO 2 , with a significant increase in CH 3 I concentration at higher pCO 2 .However, without additional empirical measurements, it is unclear whether this decrease was caused by bacterial methyl transferase enzyme activity or by photochemical degradation at higher pCO 2 .
*Correlation is significant at the 0.05 level (two-tailed).* * Correlation is significant at the 0.01 level (two-tailed).