Alkalinity cycling and carbonate chemistry decoupling in seagrass mystify processes of acidification mitigation

The adverse conditions of acidification on sensitive marine organisms have led to the investigation of bioremediation methods as a way to abate local acidification. This phytoremediation, by macrophytes, is expected to reduce the severity of acidification in nearshore habitats on short timescales. Characterizing the efficacy of phytoremediation can be challenging as residence time, tidal mixing, freshwater input, and a limited capacity to fully constrain the carbonate system can lead to erroneous conclusions. Here, we present in situ observations of carbonate chemistry relationships to seagrass habitats by comparing dense (DG), patchy (PG), and no grass (NG) Zostera marina pools in the high intertidal experiencing intermittent flooding. High-frequency measurements of pH, alkalinity (TA), and total-CO2 elucidate extreme diel cyclicity in all parameters. The DG pool displayed frequent decoupling between pH and aragonite saturation state (Ωarg) suggesting pH-based inferences of acidification remediation by seagrass can be misinterpreted as pH and Ωarg can be independent stressors for some bivalves. Estimates show the DG pool had an integrated ΔTA of 550 μmol kg−1 over a 12 h period, which is ~ 60% > the PG and NG pools. We conclude habitats with mixed photosynthesizers (i.e., PG pool) result in less decoupling between pH and Ωarg.

The myriad biophysical factors that modify estuarine carbonate chemistry often transcend the effects of atmospheric CO 2 hydrolysis in seawater (ocean acidification). These include the effects of groundwater flux, fluvial inputs, enhanced biological metabolism, eutrophication, upwelling, and tidal pumping, which interact in complexity resulting in coastal acidification [1][2][3][4] . The synthesis of these processes is a long-term pH variability that is estimated to be ~ 20 × greater than the open-ocean, where the increasing baseline of dissolved CO 2 magnifies the frequency and duration of carbonate chemistry extremes resulting in impeded growth and development of calcifying organisms 1,[5][6][7][8][9] . The deleterious socioeconomic implications of acidification has led to policy initiatives aimed at utilizing phytoremediation (i.e., photosynthetic CO 2 uptake) by seagrass and kelp to locally mitigate acidification events [10][11][12] . This assumes that photosynthesis by macrophytes can reduce the dissolved inorganic carbon (TCO 2 )-simultaneously raising pH-during daylight hours when photosynthetic rates are high relative to heterotrophic respiration in seagrass beds and kelp forests. Initial research on this topic found that daytime reduction of TCO 2 by seagrass is capable of increasing pH on short time scales, however residence time, depth, and enhanced community metabolism in nearshore seagrass habitats were found to dampen mitigation or exacerbate extreme conditions offering only minor, temporary, refuge from acidification 9,13-17 . These equivocal conclusions of carbonate chemistry variability in seagrass habitats may partially explain the contrasting correlations between bivalve growth and proximity to seagrass patches 18,19 . Notwithstanding the emerging complexity of phytoremediation, it is clear that further studies are needed to investigate the habitat specificity as it relates to biological communities and the physicochemical oceanographic dynamics of seagrass and kelp ecosystems from an acidification context.
To quantify phytoremediation by seagrass the carbonate system needs to be properly constrained as organismal sensitivities to acidification are specific to individual parameters (e.g., pH and CaCO 3 saturation state Ω)-acidification is a multi-stressor 20,21 . Complicating matters is the nuance of carbonate chemistry variability in coastal margins where the potential for specific parameters to diverge from co-varying positive correlations (i.e., pH and Ω) is high, a phenomenon referred to as a decoupling of the carbonate system 1,22 . Previous studies have examined seagrass phytoremediation via autonomous pH and O 2 sensors complemented by periodic discrete sampling of TCO 2 or TA (total alkalinity) 9,15,17,18,23 , however logistics including site accessibility, timing of tidal cycles, and ability to conduct high-frequency sampling often precludes properly constraining the carbonate system. This can lead to the potential for measurement-estimation discrepancies 24 , which can equivocate occurrences of carbonate parameter decoupling and quantification of phytoremediation.
To date, most phytoremediation analyses from observations and modelling rely heavily on positive correlations between pH and seagrass density as a means to identify the potential for acidification mitigation 13,16,17 . Conclusions regarding acidification amelioration are, thus, limited by assumptions of a coupled carbonate system and an opacity to detail the multi-stressor component. In this study, we characterize the carbonate chemistry of adjacent pools in the high intertidal defined as being dense, patchy, or devoid of seagrass (Zostera marina). We measured multiple carbonate chemistry parameters (pH, TCO 2 , and TA) in each pool over a 17-d period at high frequency to identify tidal and diurnal patterns of carbonate chemistry change as a function of the presence and abundance of seagrass. Our analysis highlights the frequency of carbonate chemistry decoupling of pH and Ω arg as it relates to seagrass density and TA variability. If this decoupling is common in seagrass beds, then previous estimates of phytoremediation are potentially overestimated due to assumptions about positive correlations among parameters (e.g., pH, Ω arg ) despite the use of a robust TA-salinity relationship in calculating carbonate chemistry variables.

Results
Timeseries of pool carbonate chemistry. Observations recorded in dense grass (DG: 62% of pool area), patchy grass (PG: 26% of pool area), and no grass (NG: 0% of pool area) pools at the head of Jakolof Bay, AK (Fig. S1), displayed robust hourly changes in TA, TCO 2 and pH from 15-27 June (Fig. 1). An increasing dynamic range of ΔTA correlated with residence time, and to a more moderate degree, with ΔTCO 2 (Fig. S2). Autocorrelation at lag of 2-corresponding to the troughs of the TA timeseries-was significant for the DG (p = 0.013), PG (p = 0.023), and NG (p = 0.002) pools. Immersion time (i.e., period pools were flooded) decreased from 3.85 to 2.60 h while depth of overlying water at high tide decreased from 1.18 to 0.30 m during the spring to neap tidal transition increasing the magnitude of carbonate chemistry change (Fig. 1). Over the 17-d period the ΔTA (μmol kg −1 h −1 ) range was greatest in the DG pool with a maximum value 43% greater than the PG pool, and 26% greater than the NG pool (Table S1). The ΔTCO 2 maximum rate in the DG pool was double that of its ΔTA and only 23% and 48% greater than the PG and NG pools, respectively (Table S1). Immediately following each flood cycle when pools were emersed and retained an average depth of 6 cm, the TA, TCO 2 , and pH T signals were approximately equal to ocean measurements and similar to normative estuarine systems. This is despite extremely low salinity (Fig. S3) at the surficial layer of the incoming flood tide which lowered ocean TA only at the surface. Small fluctuations in pool salinity (≤ 1), however, correlated well (slope = − 0.466; R 2 = 0.849) with changes in depth (cm) which ranged between 1-2 cm when using the NG pool as reference.
Estimated pH T calculated from TCO 2 and TA in all pools were robustly different from direct pH T measurements resulting in a measurement-estimation discrepancy (Fig. 1c-e). Measured values were consistently higher where the mean of pH T -pH T_est (± SD) was 0.38 ± 0.35 for DG, 0.22 ± 0.26 for PG, and 0.33 ± 0.23 for NG pools. The NG pool flooded at a height 0.23 m higher than DG and PG pools resulting in an extended emersion period and complete evaporation of the pool on 26 June producing anomalous measurements after the 24th as robust deviations became present (Fig. S3). The PG pool had the greatest overall pH T range from 7.64 to 9.25 while the daily extremes were slightly less from 7.64 to 9.14, and 7.65 to 9.08 for the DG and NG pool, respectively. The daily increase in pH T occurred concomitantly with temperature that ranged from ~ 12.4 to 26.6 ( Fig. S3), which would thermodynamically decrease pH T by ~ 0.225 units over the TA and salinity values observed due to the positive correlation between temperature and carbonic acid dissociation constants.
Hourly rates of change during emersion. High-frequency sampling of carbonate chemistry and ancillary parameters (O 2 , temperature, salinity, and nutrients) characterize a diel modulation for all pools with increases in TA and TCO 2 at night (PAR < 100 μmol photons m −2 s −1 ) and decreases during the day (Fig. 2a-c). Hourly nighttime increases in TA and TCO 2 for DG and PG pools were 42.13 and 48.50 (R 2 = 0.99 and 0.98), and 44.99 and 173.08 (R 2 = 0.99 and 0.92) μmol kg −1 h −1 , respectively. The ratio at which TA and TCO 2 increased for the DG (1.07) and PG (1.14) pools was ~ 1 whereas the NG pool had a TA:TCO 2 ratio of 1.84. In daytime, TA decreased linearly for all pools at a rate ~ 51.0 μmol kg −1 h −1 (R 2 = 0.98) for DG and NG pools, and 32.3 (R 2 = 0.97) μmol kg −1 h −1 for the PG pool. TCO 2 decreased fastest in the PG pool resulting in higher pH T earlier in the day compared to DG and NG pools, and a more rapid shift in carbonate chemistry speciation from HCO 3 − to CO 3 2− . Supersaturation of CaCO 3 (Ω arg ) persisted in all pools for the entire emersion period (~ 21 h) regardless of PAR levels ( Fig. 2d-f). Estimates of TCO 2 modification attributable to photosynthesis and respiration as well as CaCO 3 precipitation or dissolution-estimated from changes in TA-show that respiration and photosynthesis was the predominate mechanism of ΔTCO 2 . The degree of ΔTCO 2 appeared to far outpace ΔO 2 , which peaked in late morning.
Alkalinity drawdown and associations with seagrass. Logistical curve fits to ΔTA as a function of emersion time was greatest in the DG pool reaching a maximum of ~ 550 μmol kg −1 (RMSE = 82.3) around 10.5 h compared to the NG (RMSE = 46.4) and PG (RMSE = 58.0) pools with ΔTA maxima of ~ 300 μmol kg −1 at 8.5 h (Fig. 3a). At maximum ΔTA, DG was significantly different than both PG and NG pools represented by nonoverlapping model bounds. The ΔTA per proportion of seagrass cover over the same emersion period appeared greater in the PG pool relative to the DG pool, however, the large RMSE (DG = 133.3 and PG = 215.5) bounds suggests these two pools are undistinguishable (Fig. 3b). relationships with pH T varied by pool for the entire timeseries. A decoupling from a consistent positive correlation between pH T and Ω arg was observed in the DG and PG pools which displayed Ω arg < 1.5 across a pH T range 7.63-9.10, with a greater proportion of low Ω arg values at high pH T in the DG pool relative to the PG pool (Fig. 4)  www.nature.com/scientificreports/ Measured TA and TCO 2 deviated from estimated values when using two auxiliary carbonate system variables, corroborating decoupling between pH T and Ω arg in all pools. Estimated TA was predominately greater in all pools ranging from 1049 to − 53, 1063 to − 92, and 813 to 18 μmol kg −1 in the DG, PG, and NG pools, respectively (Fig. 5). The converse was true for TCO 2 where measured values were majority greater than estimated values. The TA estimates derived from the TA-salinity regression were modest relative to measured values, with ranges below 200 μmol kg −1 for the DG and PG pools, and ~ 450 μmol kg −1 for the NG pool (Fig. 5). We note that the R 2 was poor for the DG and PG pools and only moderate in the NG pool (Fig. S4). TCO 2 derived values calculated from an estimated TA based on regression with salinity approximately followed TCO 2 estimated from measured pH T and TA. Discrepancies as great as ~ 250 μmol kg −1 , however, were still observed (Fig. 5). For all estimated values, the timepoints that are most congruent with actual measured values occur at the peaks of the timeseries. These were periods immediately following the flood tide where the more homogenous oceanic signal replaced local pool carbonate chemistry dynamics.
( 1 2 ( 1 2 h   , and CO 3 2are marked as grey on the right y-axis with colored pH T isoclines. Absolute values of ΔTCO 2 and ΔO 2 during same emersion period where the total ΔTCO 2 was estimated based on proportion of change due to biological respiration/photosynthesis or CaCO 3 precipitation/dissolution for dense grass (d), patchy grass (e), and no grass (f). Isoclines are Ω arg . Note: The NG pool during this period began to experience increased salinity due to evaporation reducing confidence in the displayed values.

Discussion
The extreme diel cyclicity of TA observed in this study is unprecedented for nearshore seagrass habitats in temperate locations and refutes assumptions of its invariability and strong correlation with salinity, a relationship often used to constrain the carbonate system. The modulation of pH T , TCO 2 , and TA in each of the pools exceeds those that would be derived based on any two of the carbonate chemistry parameters resulting in measurement-estimation discrepancies and an inability to accurately quantify a decoupled system-a situation likely overlooked by previous studies [15][16][17]23,25 . Extreme decoupling of the carbonate system was present in the DG pool only, where pH T ranged from 7.65 to 9.19 while maintaining a salinity > 26 and Ω arg < 1.5-a threshold at which acute stress occurs in certain bivalve larva 26 . The two seagrass pools (DG, PG) displayed fundamental differences as it relates to extremes in carbonate chemistry variability, characteristic of previous findings detailing an exacerbation of extremes in seagrass habitats 9 . Despite abundant filamentous macroalgae and observed microphytobenthos (Fig. S1), the NG pool exhibited a reduced magnitude of variability and maintained a mostly positive correlation between pH T and Ω arg . The OC signal experienced more modest decoupling, however this was due to the freshwater lens at the surface upon the incoming flood tide. While phytoremediation may appear present during occasions with extremely high pH T and Ω arg , the reduction of TCO 2 and bioavailable carbon for calcification remained extremely low, potentially impeding organismal calcification [27][28][29] , inducing a result opposite of phytoremediation. While these conclusions are based on in situ timeseries sampling without replication, the consistent behavior and difference between each pool and autocorrelation over the timeseries gives confidence in our conclusions.
Model estimates of daytime ΔTA as a function of residence time suggest that the mixed autotroph PG pool resulted in a lower integrated TA decrease but a faster rate of TCO 2 drawdown shifting the distribution of carbonate chemistry speciation to limited CO 2 availability earlier in time (Fig. 6). Based on our results, we hypothesize that higher photosynthetic rates by non-seagrass photosynthesizers (e.g., microphytobenthos) in mixed seagrass communities can raise pH and drawdown TCO 2 faster leading to a more rapid increase in TA:TCO 2 due to the TCO 2 uptake physiology by those autotrophs 14,30,31 . This is counter to other assertions suggesting greater seagrass density (leaf area index) leads to a greater potential of acidification remediation 13 ; it is clear though, that a more rigorous characterization of the carbonate system is needed to address the efficacy of mitigation and potential decoupling of the system as demonstrated by this study.
The effects of extreme TA diel cycling modify the acid-base chemistry and, thus, the sensitivity of Ω arg , pH, and PCO 2 to subsequent fluctuations in TA and TCO 2 32 . The TA:TCO 2 ratio ranged from 1.05 to 1.80 with highs c. e.
f. www.nature.com/scientificreports/ correlated to longer residence times during neap tidal periods that affected the duration of immersion and emersion. Studies that have previously recorded such changes in TA identify benthic flux or CaCO 3 dissolution as the driver of diel variability, however the attributes of the sediment in those habitats were permeable, medium sand or coarse, and rich in CaCO 3 -conducive conditions for enhanced diffusive and advective efflux from porewater [33][34][35] . While decreases in TA can be a result of calcification by epibionts or seagrass leaves themselves, those instances occurred in tropical environments with waters extremely high in CaCO 3 , or in temperate nearshore waters where riverine inputs carried high [TCO2] and [TA], and Ω arg > 10 in the submerged aquatic habitats; however, neither reported diel cycling of TA or found the unique TA:TCO 2 ratios observed here 36,37 . In this study site, the sediment in the study pools was comprised of slate and greywacke, comingled with densely packed fine-grained clay and silt, attenuating in-sediment permeability. Porewater profiles at 1, 2, and 3 cm depths depicted [TCO 2 ] > [TA Carb ] and were consistently higher than the concentrations in the overlying water (Fig. S5). Given this orientation, efflux of TA and TCO 2 from porewater should be persistent, particularly as the concentration gradient would increase during the day as TA and TCO 2 decreased in the pools. If we assume the solute exchange between porewater and overlying water was the mechanism for observed diel TA variability, we can estimate an integrated benthic flux at night in the DG pool of 4.4 mmol m −2 (~ 6 h) and ~ 10 mmol m −2 (~ 12 h) during the day, with daytime rates for the PG and NG pools slightly lower at ~ 5.5 mmol m −2 . These rate estimates are similar to those reported in tropical environments where TA flux occurs concomitantly with dissolution in permeable sediments 33 . There was no evidence of high CaCO 3 in the muddy sediments at this site, however, nor of calcifying epiphytes as this region is dominated by cyanobacteria and diatoms at the sediment surface 38 -epiphytic growth, overall, was surprisingly minimal. The linear changes in TA over the 21 h period would assume a diffusive flux with a likely stagnant boundary layer because advective processes that can enhance flux rates were limited to bio-irrigation and-turbation-which visually appeared minimal-due to lack of other forces (e.g., wave, current, tide). The characteristics of TA variability were expressed as linear rates of change during the day and at night, whereas TCO 2 changes were nonlinear during the day and linear at night. At night TA and TCO 2 increased ~ 1:1 in the DG and PG pools, which exemplified a possible scenario of CaCO 3 dissolution (2:1 change) coupled with respiration that would change TA:TCO 2 0:1. If plausible, this would have to occur in superstrated waters (Ω arg was > 1) where the ΔO 2 roughly matches the estimated-respiration only-ΔTCO 2 . This was not the case, however, as the ΔTCO 2 was < ΔO 2 after 3 h (ratio of 0.55 and 0.44, respectively) and mixed after 6 h with a ratio of 0.75 and 2.0 in the DG and PG pools, respectively. It is possible denitrification-nitrification processes could account for this excess O 2 by lowering the community respiration quotient as has been seen in seagrass communities 39 . While we note that biogenic CaCO 3 dissolution occurring at Ω arg > 1 is possible, the rate of dissolution is minimal in supersaturated waters and dependent on specific polymorphs 40 . Additionally, the rate of ΔTA is consistent despite the temperature fluctuation in the pools, which would enhance the rate of dissolution increasing the rate of TA change: this was not observed. These www.nature.com/scientificreports/ speculations for TA variability of course assume ΔTCO 2 could be partitioned by precipitation/dissolution, of which there is no strong evidence. Nutrient assimilation and remineralization as well as organic alkalinity can also contribute to changes in TA [41][42][43][44][45] , but not at the scale of change observed here. Over the high frequency sampling period when nutrients were measured, the stochasticity and low magnitude of change in PO 4 3− , SiO 2 , NO x , and NH 4 + were not found to correlate with ΔTA (Table S2). The changes in TA observed were 1-2 orders of magnitude greater than changes in nutrient concentrations resulting in a trivial addition to ΔTA. In addition, presence of organic alkalinity derived from phytoplankton or humic organic compounds would result in measured TA values > estimated values, but this was not the case. This further complicates the identification of processes responsible for TA variability and, thus, provokes the speculation of non-dissolution and nutrient cycling mechanisms.
The modulation of TA and TCO 2 at a 1:1 ratio during night and a decreasing ratio during the day as carbon becomes potentially limiting for seagrass gives credence to HCO 3 as a potential source of TA cycling. Specific seagrass species including Z. marina and other macrophytes are known to utilize HCO 3 as a carbon source [46][47][48] . Evidence suggests the active uptake of HCO 3 − occurs via H + symport in P. oceanica, where electroneutrality is likely preserved by a Cl − or NO 3 − efflux and Na + /H + antiport 49,50 . The accumulation of HCO 3 in P. oceanica aids in the establishment of a robust electronegative potential in the leaves, which is also a phenomenon present in Z. marina 50 . The accumulation of HCO 3 within the cell wall may occur at a faster rate than the dehydration to CO 2 in the cytoplast catalyzed by carbonic anhydrase, which could lead to efflux of undehydrated HCO 3 − at night when light energy is limiting. This could also explain the disparity between O 2 generation and TCO 2 drawdown during the day as hysteresis can occur on the timescale of hours 51 , which could be further modified by photorespiration 52 . The evidence here, along with the suggested mechanisms by which electroneutrality is preserved when HCO 3 − uptake occurs could explain the decrease in TA observed in these pools when TCO 2 is limiting. Photosynthesis, however, is not presumed to affect TA even if HCO 3 − is utilized because it is expected that uptake would be compensated with H + or OH − exchange 43 . More evidence is needed though to determine if this is the case in higher order photosynthesizers because research shows electroneutrality preservation by OH − and H + may be replaced by NA + , Cl − and NO 3 − in some seagrasses 48,49,53 . Anomalous to this conclusion would be the observed TA variability in the NG pool. The Ulva spp., which was observed in the NG pool, however, can also take up HCO 3 − via ion exchange, potentially with OHor Cl −47,54 . While further investigation is needed to identify the mechanism of TA variability in these pools, similarly low TA values and cycling have been recorded in enclosed bays with long residence times and abundant seagrass, and even speculation of HCO 3 was noted as the potential driver of the observed TA variability 35,52,55 . These incidences of low TA and its diel cycling, however, were not assessed from a phytoremediation standpoint, thus the implications hitherto remained unappreciated.
The pools in this study are representative microcosms of larger systems, replicating carbonate chemistry variability in seagrass habitats on a magnified scale. Perched estuaries, lagoons, and enclosed bays with long residence times have recorded extremely high pH values similar to those found in this study, including instances of reduced TA: correlated to the proximity of oceanic influence 52,55,56 . In these systems, biological metabolism and evaporation become the dominate mechanisms that modify pH 5,56,57 . It would be remiss to note, however, that the thermodynamic controls on carbonate chemistry also become enhanced at long residence times as was seen in this study. Observed temperature fluctuations ranged from ~ 12.5-26.5 °C increasing the carbonic acid dissociation constants resulting in an estimated pH drop of ~ 0.21 units across the recorded pH and TA range (Fig. S2); however, this was superseded by photosynthetic modification of pH. Evaporation appeared to have little effect on the DG and PG pools with respect to salinity as values remained fairly constant even at extreme temperatures (Fig. S2). Noticeable was the complete evaporation of the NG pool and the rapid salinity increase, suggesting that small variations in the volume of tidal immersion (i.e., depth of overlying water) can modulate the degree to which estuary carbonate chemistry is affected by the slope of the tidal region.
Findings here show unequivocal, frequent, decoupling of carbonate chemistry that would otherwise be overlooked without properly constraining the system and absolving measurement-estimation discrepancies. This can lead to an overestimation of phytoremediation when conclusions are based on pH variability rather than the total carbonate acid-base chemistry system 17,23 . This can occur despite a robust TA-salinity relationship or because of a mischaracterization of TA variability if results are derived from discrete measurements based on specific sampling times corresponding to tidal period, proximity to macrophyte habitat (above or in canopy) and coupled with pH-only monitoring. In accordance with previous studies, findings here show that long residence times and spatial variability along with tidal and current mixing are strong drivers for determining carbonate chemistry variability in seagrass 13,15 , however, we show that decoupling of the carbonate system in dense seagrass occurs rapidly, is independent of low salinity, and is likely related to extreme TA variability potentially caused by a hysteresis of how HCO 3 cycles within the medium in a carbon-limited system.

Materials and methods
Site description and assessment. Jakolof Bay is located in the outer portion of Kachemak Bay where local oceanographic conditions and carbonate chemistry are driven by exogenous characteristics from the Gulf of Alaska and autochthonous biological metabolism 58 . Jakolof Bay is a small fjord (3.5 km in length) that opens up into Kasitsna Bay, fed terrestrially by Jakolof Creek which runs along the north and south boarding the elevated salt marsh and the higher tidal flat-interspersed with depressions-where study site pools were located. The topography of the site suggests that minimal terrestrial subterranean groundwater reaches the pools which are at elevation from the land side creek. Thus, porewater intrusion likely originates from the oceanic front during the floodtide pressure gradient. The geology of Jakolof Bay consists primarily of highly metamorphosed slate and graywacke, likely from the Triassic Period 59 . The sediment in each pool was muddy with interspersed slate gravel. The outer region of Jakolof Bay sediment is ~ 60% fine grained silt and clay 60  www.nature.com/scientificreports/ characteristic to that found in the pools. Species characterization of the intertidal in Jakolof is scarce, but shallow subtidal assessments identified dominant taxa as Polychaetes, Malacostraca, Gastropods, and Bivalves, however, the diversity of these groups was fairly low relative to other fjords in the region and the deeper areas of Jakolof Bay 60 . Pacific blue mussels (Mytilus trossulus) were observed in the creek channels, while scattered amphipods and sparse Littorina spp. feeding on the fleshy macroalgae appeared to be the only potential calcifiers in the pools, which were transported in-and-out during flood and ebb. This was the extent of the fauna characterization, although presence appeared to be minimal as well as epiphytic growth on seagrass (Fig. S1).
Sample collection and processing. Three shallow, adjacent pools with varying depth on the edges, within 50 m of one another were selected as sample sites and characterized as dense grass (DG), patchy grass (PG), and no grass (NG) with ellipse areas ~ 330.9, 180.0, 339.9 m 2 with average center depths 5.1, 6.2, and 7.1 cm, respectively, in the high intertidal of Jakolof Bay, AK: 59°26′54.09″ N, 151°29′49.96″ W (Fig. S1) batch #181) measured before and after each machine calibrated run. pH T was measured potentiometrically with a Thermo Scientific ROSS Ultra electrode calibrated at total scale with Tris buffer and corrected with an offset that was derived from a regression of 25 samples between potentiometric and spectrophotometric measurements using a Shimadzu UV-1900: this offset was 0.019 units (Fig. S5). O 2 measurements were performed with a PreSens Fibox 4 (using factory calibration) after each sample was collected and immediately stored in a dark box in the field until measurement ~ 30 min later. Salinity was measured with a YSI 3100 conductivity meter. All TCO 2 samples were run at Shannon Point Marine Center, WA, on an Apollo SciTech AS-C3 along with several CRMs (batch #179) interspersed after calibration. Each TCO 2 measurement reported was the average of the three closest analytical measurements that were < 10 μmol kg −1 between each measurement. The uncertainty for measured TA (7.58 ± 8.78 SD) and TCO 2 (6.77 ± 6.32 SD) was the average difference between known CRM and measured CRM across all samples. Estimated pH T and Ω arg were calculated using CO2SYS (Matlab V1.1) with inputs TA and TCO 2 using the carbonic acid dissociation constants from Lueker et al. 61 , the bisulfate dissociation constant of Dickson et al. 62 , and the boron constant from Uppström 63 . Assuming the ΔTCO 2 over the 21 h sampling period was a response to photosynthesis/respiration and CaCO 3 precipitation/dissolution, estimates of partitioned ΔTCO 2 were calculated using the absolute hourly rate of change for TCO 2 and TA during each time point. Where ΔTA*0.5 (based on the alkalinity anomaly) was equal to the ΔTCO 2 as a result of precipitation or dissolution, and the remainder of ΔTCO2-ΔTA*0.5 was a due to biological metabolism. Proportion of cover was calculated by measuring the length and width of each pool and then using photographed images to define the proportion of pool area covered by Z. marina present as a ratio of pool size using ImageJ (v. 1.53a). Significance of autocorrelation lag points on TA timeseries for each pool was determined using a Ljung-Box Q-test.

Model construction.
A three-parameter logistic curve fitting routine was applied to each pool correlating ΔTA with emersion time when samples were collected immediately after and before flood tide. This ended up being 12 time points for DG and PG pools and 10 for the NG pool (pool evaporated at day 15) during the change in tidal cycle from spring to neap. A conceptual model of carbonate chemistry dynamics for the DG and PG pools was determined by using the estimated values of ΔTA across the entire time series (described above) and the changes in carbonate chemistry speciation derived from the high frequency 21 h sampling period. Since the ΔTA during the 21 h sampling period was integrated into the entire timeseries estimates, the carbonate speciation changes are representative of the expected dynamics that would be visible at other time points.
Porewater sampling. Porewater collectors were assembled using Super Speedfit polypropylene 6.35 mm press-connect fittings. T-shaped connectors were fit with two, ~ 3.8 cm length pieces of food grade plastic tubing, with open ends sealed with thermoplastic hot melt adhesive. Two sides of each piece of tubing were punctured five times with a 16-gauge needle, wrapped with a 0.45 micron PES membrane filter and adhered with thermoplastic adhesive to keep out sediment. Three collectors for each pool were buried at 1, 2, and 3 cm depths (Fig. S1), ~ 36 h and 3 tidal cycles before the first samples were collected. The top of each T-connector-which protruded above the sediment-was sealed with a Super Speedfit polypropylene plug.
Prior to collection, 5 mL centrifugal tubes were placed in a glove bag purged of O 2 and filled with N 2 . Vials sat in a glove bag with caps off for 1-2 h while being filled with N 2 and shaken haphazardly. The caps of each vial had a 6.35 mm hole drilled in the top and then covered with electrical tape. Caps were secured from inside glove bag and vials then stored and transported in a plastic bag. A 10 mL serological pipette fitted with a 6.35 mm piece of rigid tubing was fit into the top of each press-connect securing a tight connection and porewater slowly extracted. The first 2 mL of water was discarded and 4-5 mL transferred to the vial by removing tape temporarily and injecting the collected porewater into the vial. Samples were measured immediate for pH T in glove bag using a Thermo Scientific ROSS Ultra electrode calibrated with Tris buffer and reported on the total scale. A 0.019 correction factor derived from a 25-sample regression between potentiometric and spectrophotometric measurements using a Shimadzu UV-1900 was applied. After pH measurement, samples were poisoned with www.nature.com/scientificreports/ Publisher's note Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
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