Coastal ocean acidification research is dominated by laboratory-based studies that cannot necessarily predict real-world ecosystem response given its complexity. We enriched coastal sediments with increasing quantities of organic matter in the field to identify the effects of eutrophication-induced acidification on benthic structure and function, and assess whether biogenic calcium carbonate (CaCO3) would alter the response. Along the eutrophication gradient we observed declines in macrofauna biodiversity and impaired benthic net primary productivity and sediment nutrient cycling. CaCO3 addition did not alter the macrofauna community response, but significantly dampened negative effects on function (e.g. net autotrophy occurred at higher levels of organic matter enrichment in +CaCO3 treatments than −CaCO3 (1400 vs 950 g dw m−2)). By identifying the links between eutrophication, sediment biogeochemistry and benthic ecosystem structure and function in situ, our study represents a crucial step forward in understanding the ecological effects of coastal acidification and the role of biogenic CaCO3 in moderating responses.
Acidification of seawater via the increasing absorption of atmospheric CO2 (ocean acidification; OA) is a key contemporary issue for the marine environment1. However, eutrophication-induced acidification2 has received comparatively little attention, despite affecting vast portions of the world’s coastal zones3. Eutrophication is defined as an increase in the rate of supply of organic carbon to an ecosystem and occurs in coastal waters primarily via the anthropogenic input of excess nutrients4. Excess nutrients promote short-lived algal blooms which, upon collapsing, are deposited to the benthos5 where microbially-driven aerobic respiration of organic matter releases CO2 in approximate equivalence to O2 consumption6, causing localised acidification7. In highly productive estuarine environments, eutrophication-induced acidification adds variation to background fluctuations in pH driven by changing rates of respiration and photosynthesis8,9 and watershed effects10, and occurs against a backdrop of global OA that is set to reduce seawater pH 0.3–0.4 units by 210011. The co-occurrence of these acidification pathways means coastal environments may experience decreases in seawater pH far exceeding those predicted from OA alone12,13,14. Additionally, biogeochemical changes associated with aerobic (i.e., O2 depletion) and anaerobic (i.e., dissimilatory N and S reduction) pathways of benthic organic matter degradation mean that acidification rarely acts in isolation, but is rather a single component in a multi-stressor setting also comprising hypoxia and increased concentrations of toxic solutes15,16.
Coastal benthic macrofauna communities exhibit predictable responses to organic matter enrichment, such as reduced abundance and diversity at high levels of loading17. These responses are usually attributed to the onset of hypoxia3, however empirical evidence suggests some organisms respond more strongly to fluctuations in pH than O2 (e.g. juvenile clams)18. Whilst it is generally accepted that calcifying organisms will fare poorly under acidification due to calcium carbonate (CaCO3) under-saturation and increased likelihood of dissolution19,20,21, the consequences for non-calcifying organisms are less certain and vary interspecifically22. Understanding the response of benthic communities to decreasing pH is critical, as numerous ecosystem services (e.g. food production and nutrient cycling) are underpinned by functions (e.g. primary production and organic matter mineralisation) that are strongly influenced by resident macrofauna23,24. Evidence from laboratory experiments suggests that processes such as denitrification may be disrupted by decreases in seawater pH, owing to a breakdown in the facilitative interactions between macrofauna and denitrifying bacteria25,26. Naturally occurring gradients of acidification have been utilised to investigate the effects on benthic communities in the field, for example by monitoring communities with increasing distance from shallow volcanic CO2 vents27,28,29. Whilst these studies have provided insights into potential changes in community structure, including decreases in the abundance of calcareous organisms, and even evolutionary adaptations, there are frequently additional environmental variables that co-vary along the gradient (such as temperature and toxic trace elements) making it difficult to attribute the responses to acidification alone30.
The difficulty in conducting controlled acidification experiments in situ has meant benthic OA research has tended towards laboratory-based studies often using simplified biological communities or individual species. Of the 324 studies published by 2014 on marine organisms’ responses to reduced coastal pH, three quarters were conducted in the laboratory31. Whilst laboratory-based studies provide a controlled mechanistic understanding of acidification effects, they cannot predict in situ ecological responses given the complexity of natural ecosystems. For example, the ability for mobile organisms to disperse from impacted sediments32 is inhibited when entire experimental units (e.g. cores or mesocosms) are acidified, but this is a crucially important behavioural trait providing resilience to benthic communities when considered at landscape or ecosystem scales33,34. Recent OA field studies have also highlighted how functional redundancy in benthic communities may provide resilience against acidification which would otherwise be masked in low diversity laboratory studies. Baggini et al.35 documented a switch in the main grazer of macroalgae from sea urchins to fishes along a gradient of increasing CO2 concentration, preventing a phase shift from an ecosystem dominated by encrusting algae to macroalgae. Numerous laboratory studies have previously identified positive responses of marine autotrophs to increased CO2 (see36), but this may not be observed in situ if species replacement maintains grazing pressure.
Furthermore, laboratory experiments frequently neglect the multi-stressor nature of benthic acidification (the usual mechanism for reducing seawater pH is via the bubbling of CO2 gas37,38, shifting water column pH only), and the natural buffering capacity of the coastal environment may be overlooked or poorly replicated in artificial settings. To make empirical studies more relevant to the real-world, Hewitt et al.39 advocate conducting field experiments across environmental gradients to address scaling issues between the understanding gleaned from simplified small-scale laboratory experiments and the response of diverse large-scale ecosystems40,41.
The complex biogeochemistry of the coastal zone is likely to affect ecological responses to acidification. Coastal ocean sediments contain approximately 50% of oceanic CaCO3 deposits, originating in temperate regions mostly from bivalve shells and bryozoan skeletons42. CaCO3 minerals dissolve in response to increased acidity from CO2 hydrolysis, according to equations (i) and (ii).
When CO2 hydrolysis and CaCO3 dissolution are coupled in this way, there is no net change in hydronium ion (H3O+) concentration and thus no change in pH (pH = −log[H3O+]), although buffering capacity, i.e. the ability to neutralise H3O+, increases according to the increase in HCO3− 43. The porewaters of CaCO3-rich coastal sediments may therefore possess high buffering capacities44,45 which reduce the potential for significant fluctuations in pH. CaCO3 has even been suggested as a tool to prevent the negative effects of localised benthic acidification46. Whilst Green et al.47 observed a three-fold increase in bivalve recruitment in cores buffered with crushed shell hash, Greiner et al.48 observed no such effect in similarly buffered plots, despite significant increases in porewater pH. To date, the only field study investigating the link between benthic acidification, CaCO3 buffering and ecosystem function was inconclusive due to heterogeneity in the environment49. It is necessary to clarify the nature of these linkages as intensifying coastal acidification may remove the key species that consolidate CaCO3 into sediments50 and lead to dissolution of existing CaCO3 deposits51, such that any resilience provided by CaCO3 buffering to ecosystem functioning will be lost.
In this study, the ability of biogenic CaCO3 to maintain intertidal benthic ecosystem structure and function along a gradient of eutrophication-induced acidification was investigated in situ. Organic matter enrichment treatments (0–2250 g dw m−2, increasing in 250 g increments) formed the eutrophication gradient, and enriched plots (1.44 m2) were allocated one of two CaCO3 treatments (with or without the addition of 2000 g m−2, i.e. +CaCO3 or −CaCO3 treatments). After 70 d of enrichment we assessed treatment effects on sediment properties, macrofauna community structure and key ecosystem functions (e.g. net primary production and nutrient processing), which were derived from solute fluxes across the sediment–water boundary measured in light and dark benthic incubation chambers. The presumed mechanism by which CaCO3 would increase resilience was through reducing the range of pH variability via buffering of CO2 (Eqs 1 and 2). As such, it was hypothesised that sediments with abundant CaCO3 would experience less extreme fluctuations in pH than those without when mineralising excess organic matter to CO2. If fluctuating pH was the primary eutrophication-induced stressor, the macrofauna community was expected to be less affected by organic matter enrichment when there was excess CaCO3, helping to maintain ecosystem function. Conversely, a lack of a positive effect of CaCO3 could indicate that additional eutrophication-induced stressors (hypoxia, H2S toxicity) were more important regulators.
To test our predictions, one-way PERMANOVA (using the PERMANOVA + package of Primer V7) were performed with CaCO3 treatment considered a fixed factor and organic matter treatment a continuous co-variable. This approach allowed assessment of the interactive effects of organic matter and CaCO3 treatments on response variables. Some ecosystem functions were variable yet significantly correlated with organic matter treatment, therefore multiple regression (using distance-based linear models (DistLM) in Primer V7) was also performed to determine environmental drivers (e.g. sediment properties, macrofauna community structure) of this variability.
Seventy days after manipulation, surface sediment characteristics (0–2 cm) were similar between plots (Table 1) and any effects of the disturbance caused by treatment establishment had subsided (see Supplementary Information for ambient and control treatment comparisons). Only phaeopigments, a product of chlorophyll degradation, showed a relatively large range (2–27 µg g−1 dw) driven by high values in organically enriched plots. At 2–5 cm sediment depth (organic matter and CaCO3 were added at a depth of 5 cm) a significant elevation of CaCO3 content in +CaCO3 treatments (1.4%) versus −CaCO3 treatments (0.5%) (F(1, 33) = 12.81, p = 0.001; Fig. 1a) was achieved. There was no significant interactive effect between CaCO3 and organic matter treatments on organic content (OC) or porewater pH, but there was a significant effect of organic matter treatment (Table 2). We observed a linear increase in OC along the organic matter treatment gradient (r2 = 0.44, p < 0.001; Fig. 1b) with mean OC doubling from 2% in 0 g dw m−2 plots to 4% in 2250 g dw m−2 plots, and a linear decrease in porewater pH from 7.3 to 6.6 (r2 = 0.47, p < 0.001; Fig. 1c). Both OC and porewater pH exhibited high variability, particularly at the highest levels of organic matter treatment.
Macrofauna abundance data were averaged from two cores per plot, and total abundance and total number of taxa were determined per core (133 cm2). These community indices were only affected by organic matter treatment; CaCO3 treatment and its interaction with organic matter were both insignificant (Table 2). Mean total abundance decreased by 72% (r2 = 0.74, p < 0.001; Fig. 2a) and total species by 31% (r2 = 0.52, p < 0.001; Fig. 2b) along the organic matter treatment gradient.
Fluxes of dissolved solutes (oxygen (DO), ammonium (NH4+), nitrite (NO2−) and nitrate (NO3−)) across the sediment–water interface were used to derive indicators of key ecosystem functions pertaining to primary productivity (PP), community metabolism and nutrient processing: light chamber DO flux was equivalent to net PP (NPP) and dark chamber DO flux corresponded to sediment oxygen consumption (SOC; a proxy for community metabolism). Fluxes of nitrogenous compounds indicated rates of nutrient cycling, with NH4+ being the first product of organic matter mineralisation which may be further oxidised into NO2− and NO3− (combined and represented as NOx). Treatment effects were not consistent across ecosystem functions; NPP and NH4+ flux exhibited significant relationships with organic matter treatment, whereas SOC and NOx did not (Table 2). Chambers at low levels of enrichment were initially autotrophic (PP > SOC) during light incubations and became heterotrophic (SOC > PP) at higher levels of organic matter treatment (Fig. 3a). CaCO3 treatment significantly altered the response of NPP to organic matter enrichment (Table 2), with +CaCO3 plots exhibiting net autotrophy to higher levels of organic matter treatment than −CaCO3 plots (~1400 versus ~950 g dw m−2). NPP decreased significantly with increasing organic matter treatment in −CaCO3 plots (r2 = 0.77, p < 0.001), whereas the loss in productivity in +CaCO3 plots was less steep, more variable and was only marginally correlated with organic matter treatment (r2 = 0.24, p = 0.05). SOC showed no relationship with organic matter or CaCO3 treatments (Fig. 3b, Table 2) with high variability across the range of organic matter treatments.
Under light conditions natural log-transformed NH4+ flux (NH4+light) showed a significant response to organic matter treatment, but not CaCO3 or its interaction with organic matter treatment (Table 2). As organic matter enrichment increased, the rate of NH4+light efflux from sediments increased exponentially (r2 = 0.65, p = < 0.001; Fig. 3c), such that the rate of NH4+light efflux was more than 500 times greater in 2250 versus 0 g dw m−2 treatments. In light chambers, NOx (NOx light) showed a marginally significant response to CaCO3 addition (but not organic matter treatment; Table 2), with a slight decrease in net uptake (~15 µmol m−2 h−1) in +CaCO3 treatments (Fig. 3e). Under dark conditions (i.e. in the absence of microphytobenthos (MPB) uptake), there was a significant relationship between organic matter treatment and natural log-transformed NH4+ (NH4+dark) efflux which changed with CaCO3 treatment, as indicated by the significant interaction term (Table 2). In −CaCO3 treatments, efflux of NH4+dark increased exponentially as organic matter treatment increased (r2 = 0.35, p = 0.01; Fig. 3d), however this relationship was absent in +CaCO3 treatments and efflux rates were generally reduced. There was far greater variability in nutrient cycling measurements obtained under dark versus light conditions.
When constructing multiple regression models, marginal tests first identified significant (p(perm) <0.1) predictors of response variables when considered alone, and full models then determined the best combination of predictor variables after accounting for the variance attributed to organic matter treatment (organic matter treatment was always fitted first). In marginal tests, variability in ecosystem functions was correlated with several variables including organic matter treatment, sediment characteristics and macrofauna community indices (Table 3). For functions that exhibited a significant interaction between organic matter and CaCO3 treatments (NPP and NH4+dark), the −CaCO3 treatment had a greater number of significant predictors that individually explained more of the variation than the +CaCO3 treatment. When organic matter treatment was fitted first, it was the only predictor included in backwards elimination linear regression models of NPP for both CaCO3 treatments, but the amount of variance explained decreased from 76% in −CaCO3 treatments to 21% in +CaCO3 treatments. Although macrofauna total abundance and porewater pH explained large amounts of variance in NPP (−CaCO3 treatments) in marginal tests, both variables were highly correlated with organic matter treatment (r > 0.8) and were excluded from the model. The variables included in the full model of NH4+dark flux differed depending on CaCO3 treatment. A combination of organic matter treatment and sediment characteristics (CaCO3 content and phaeopigments) together explained 68% of the variance in −CaCO3 treatments, whereas only 17% of the variance was explained in the full model for +CaCO3 treatments by organic matter treatment. In marginal tests total species explained more of the variation in +CaCO3 treatments than organic matter treatment, but was excluded from the full model. For NH4+light flux, despite numerous variables being identified as significant predictors when considered alone, only two were included in the full model; organic matter treatment contributed most of the total variance explained (66 of 71%), with the remainder attributed to chlorophyll a (Chl a), an indicator of MPB abundance.
Natural fluctuations in pH may be extreme in the benthos of productive estuarine environments8, however coastal eutrophication and global OA are set to intensify acidification across varying scales of magnitude, space and time such that benthic ecosystem functions may be compromised. For the first time an in situ manipulation of porewater pH and investigation of the ability of CaCO3 to prevent negative change has shown that CaCO3 deposits may increase the functional resilience of benthic ecosystems to localised eutrophication-induced acidification.
The decline of benthic biodiversity with increasing inputs of organic matter is well-documented and usually attributed to the inducement of hypoxic conditions17,52, however the potential for co-occurring porewater acidification to drive these declines has been comparatively under-studied. The highest organic matter treatment resulted in a porewater pH of 6.6, and the loss of one third of macrofauna species and almost three quarters of total individuals. No increase in porewater pH could be detected in +CaCO3 treatments, nor any difference in the relationship between macrofauna community indices and organic matter treatment. This suggests that CaCO3 did not buffer porewater pH sufficiently to decrease the physiological stress of the organisms, or that other consequences of organic matter degradation such as hypoxia or increased [H2S] were more important in driving the macrofaunal response. The latter seems most likely, given CaCO3 dissolution under open-system conditions would serve to maintain pH within a given range, rather than drive it higher than typical pore water values43.
These biodiversity losses were associated with a predictable decrease in function, given biodiversity–ecosystem functioning relationships are frequently density-dependent53 and/or underpinned by key species54,55. NPP decreased significantly along the organic matter treatment gradient whilst NH4+light efflux increased, indicating a decrease in the utilisation of nutrients by the MPB community. Chl a biomass, a proxy for MPB abundance, showed no relationship with organic matter treatment and therefore cannot explain trends in NPP. It has been hypothesised that increased pCO2(aq) would result in increased productivity of photoautotrophs, and although most research has focussed on seagrasses and macroalgae36,56,57, increases in the PP of MPB have been observed in the laboratory following exposure to CO2-acidified seawater37,57. The unfavourable sediment conditions (low pH, low [O2]) created here may have stressed the MPB community beyond being able to take advantage of excess CO2. The decrease in abundance of macrofauna, whose activities are known to stimulate MPB PP58, may also have played a role. However, CaCO3 addition increased the resilience of NPP to these conditions. Significant increases in pH, total alkalinity (TA) and saturation states have been measured previously as a result of biogenic CaCO3 dissolution44,47,51, so the coarse methods used to measure pH changes here (pH field probe with ±0.2 pH units accuracy) may have masked finer scale alterations to porewater biogeochemistry which benefitted the MPB community. Importantly, CaCO3 addition had the effect of maintaining autotrophy of the benthic ecosystem to a considerably higher level of organic matter treatment, and this effect was strong enough to be detected amid the complexity of the field.
The response of light and dark nutrient cycling to organic matter treatment (increasing efflux of NH4+ and no response of NOx) indicates a limitation or breakdown of microbially-mediated nitrification pathways that oxidise NH4+ to NO2− and NO3−. There are several ways that organic matter treatment may have limited nitrification, for example a decrease in bioturbation and bioirrigation activity driven by the decrease in macrofaunal abundance may have reduced the availability of aerobic sediments59, which are required by microbial nitrifiers (i.e. ammonia- and nitrite-oxidisers). However, Braeckman et al.60 have previously shown that in the short-term (14 d), decreases in benthic nitrification rates under acidified conditions are mediated predominantly by changes in microbial community activity, rather than macrofaunal facilitation. Inhibition of nitrifiers at low pH may therefore be a factor, although it is expected that microbes are tolerant to considerable fluctuations in pH and Kitidis et al.61 previously found no significant decrease in nitrification rates at pH 6.1. Substrate-limitation is perhaps the most likely cause as NH3 is the true substrate for ammonia-oxidisers, yet below pH ~8.0 NH3 is present almost exclusively as NH4+ 62,63. Alternatively, biogeochemical processes such as dissimilatory NOx reduction to NH4+ may have increased [NH4+], a process which can be quantitatively more important than denitrification in organically-rich sediments64,65.
CaCO3 addition altered the relationship between nutrient cycling and organic matter treatment (in the dark only), such that there was no trend of increasing NH4+ efflux in +CaCO3 treatments. As porewater O2 would have been scarce in dark conditions (absence of photosynthesis) and CaCO3 addition had no effect on the macrofaunal community, it is unlikely that the improvement to sediment conditions that helped maintain nitrification rates was due to increasing availability of aerobic sediments. Similarly, there was no detected increase in pH with CaCO3 addition, therefore NH3 availability should be equally limiting. It seems most likely, therefore, that subtle changes to porewater biogeochemistry that were not measured played a role in improving conditions for nutrient cycling microbes. In future research it will be important to monitor a larger suite of carbonate chemistry parameters (pH, TA, dissolved inorganic carbon (DIC)) to identify the mechanisms underlying these functional responses. However, the aim of this study was to investigate whether laboratory-based theory could be applied in the field, and indeed, CaCO3 addition successfully dampened the negative effects of organic matter enrichment on nutrient cycling. This justifies further investigation of these interactions in situ and has important consequences for the functioning of coastal ecosystems, given the conversion of biologically-available nitrogen to nitrogenous gas provides resilience against further eutrophication66,67.
Whilst some ecosystem functions responded strongly to organic matter treatment, SOC showed no relationship with enrichment, OC or porewater pH. Since SOC is the net result of biological (BOD) and chemical oxygen demand (COD)68, it was hypothesised that SOC would increase with organic matter treatment due to an increased BOD of the stimulated microbial community and COD from increasing abundance of reducing substances, as has previously been reported for organically enriched sediments (e.g.69,70,71). The lack of a relationship may be explained by a ‘compensation’ in O2 consumption along the organic matter treatment gradient, whereby the gradual decrease in respiration and O2 consumption facilitated by macrofauna (due to decreasing abundance and stress-induced change in activity levels) was offset by a gradual increase in microbial respiration and COD, such that overall SOC remained constant.
In −CaCO3 treatments combinations of organic matter treatment, sediment characteristics and macrofauna community variables were important predictors of NPP and NH4+dark flux. In +CaCO3 treatments far fewer variables were significant predictors of function, though macrofauna community indices remained significant and individually explained more variation than organic matter treatment. This implies a strong facilitation of ecosystem function by the macrofauna community even when the geochemical complexities of sediments are enhanced. Organic matter treatment was the only predictor included in several full models (when fitted first), highlighting the dominant effect of this stressor on ecosystem function, however there was a substantial decrease in the variance it explained in +CaCO3 treatments compared to −CaCO3. This discrepancy may have been associated with the microbial component of the ecosystem, as it is the microbial community that converts and transforms solutes, though the macrofauna and sediment characteristics are key controllers of solute transport rates and microbial microhabitats72. Changes to porewater chemistry may also have driven the responses observed, therefore including a greater number of carbonate chemistry parameters and microbial community indicators in models may result in greater explanation of the functional response.
In this short-term, single-application experiment, CaCO3 effectively reduced the negative effects of organic matter enrichment on ecosystem function. However, over longer timeframes and repeated CaCO3 applications there may be potential effects associated with its addition. The extent of these effects will likely be dependent upon the difference in grain size between the ambient sediment and the added CaCO3, and whether this difference substantially alters grain size distribution. If so, benthic ecosystem functions could be affected as diffusive solute exchange across the sediment–seawater interface is highly dependent upon sediment permeability73, and the effects of macrofaunal bioturbation on function change along gradients of sediment grain size74. To avoid such impacts CaCO3 should be crushed or ground to match the sediment characteristics of the receiving site prior to addition, whilst keeping in mind that the dissolution rates of CaCO3 will vary as a function of grain size44.
Benthic ecosystem functions respond demonstrably to experimentally elevated organic matter and CaCO3 content in a field setting, despite complex interactions occurring between levels of biological organisation and environmental characteristics that influence function. Porewater acidification resulting from organic matter enrichment has negative effects on primary production and nutrient cycling which are dampened by the addition of biogenic CaCO3, thus increasing the resilience of the ecosystem to this stressor. The lack of a beneficial effect of CaCO3 on macrofauna biodiversity suggests other stressors associated with eutrophication (hypoxia, H2S toxicity) were stronger determinants of community structure than pH. The positive effects of CaCO3 addition may therefore be microbially mediated, and future research should focus on the combined response of macro- and microbiological communities to coastal eutrophication in situ. Developing a mechanistic understanding of how CaCO3 provides resilience to ecosystem function will be crucial, as losses of key CaCO3-producing species are likely under future coastal acidification stressors.
The experiment was conducted in the mid-intertidal zone of Tuapiro estuary (37°29.406′, 175°57.074′) within Tauranga Harbour, New Zealand. The site experiences a diurnal tidal cycle with inundation periods of ~5 h and a mean water depth ~1.2 m upon maximum inundation. Plots were established within a 12 m × 30 m (360 m2) area of homogeneous fine sand (median grain size 191 µm) with low mud (silt/clay particles <63 µm) (<5%), CaCO3 (<1%) and organic content (1.6–2.2% in un-enriched plots) (Table 1).
In austral summer (31st January 2017), forty 1.44 m2 plots were established (2 m apart) in a 10 column by 4 row array. Four replicates of each of the following three treatments were randomly allocated: ambient (no treatment), procedural control (PC; sediment disturbed mimicking treatment setup) and plots that received CaCO3 (pure crushed oyster shell, fragments <5 mm) but no organic matter (+CaCO3 (−OM)). The remaining 28 plots were randomly assigned one of nine organic matter enrichment treatments created using 250–2250 g dw m−2 of organic plant-derived slow-release garden fertiliser (treatments increasing in 250 g increments in a gradient design). Enriched plots were also assigned a CaCO3 treatment (with or without the addition of 2000 g dw m−2). Replication was carried out for the lowest (250 g m−2 (n = 3)), middle (1250 g m−2 (n = 2)) and highest (2000 (n = 2) and 2250 g m−2 (n = 3)) organic matter treatments. The materials used to create organic matter and CaCO3 treatments were chosen to mimic natural inputs to estuarine systems, whilst slow-release fertiliser ensured sustained organic matter degradation would result in alterations to the biogeochemical properties of the sediment.
Plots were excavated to 5 cm depth, taking care to minimise disruption to the sediment matrix, before evenly distributing organic matter and CaCO3 (in the +CaCO3 treatments) across plots and replacing sediment. The organic matter enrichment range was chosen to create a gradient in sediment OC that would elicit a response typical of eutrophically-stressed systems (i.e. acidified porewaters and reduced biodiversity), and represents a one-off depositional event such as a macroalgal bloom collapse. Such events are common globally (e.g.75,76) and in the wider estuary due to seasonal Ulva spp. blooms77. The level of CaCO3 enrichment elevated the average ambient content at the study site by 10x, which is representative of the use of CaCO3 as an acidification mitigation tool rather than a natural increase in CaCO3 content. Comparisons of sediment characteristics, macrofaunal community indices and benthic solute fluxes between ambient, procedural and CaCO3 control plots confirmed there was no significant effect associated with the presence of the added CaCO3 or the procedure of adding it to the sediment (see Supplementary Information).
Benthic solute fluxes and sediment properties were measured in situ after nine weeks (3rd–4th April 2017, early austral autumn), and macrofauna communities were sampled the following week (11th April 2017), allowing time for changes in the sediment biogeochemistry and macrofauna community to occur. Benthic flux incubations were conducted over two days with midday high tides. Fluxes of dissolved solutes across the sediment–water interface were measured under light and dark conditions in each plot, i.e. in the presence and absence of photosynthesis. As rates of photosynthesis vary with light intensity78, all light measurements were conducted on day one (and dark measurements on day two) so that chambers experienced the same light regime79. One ambient plot was dropped from the analysis due to a chamber malfunction.
The operation of the incubation chambers used for measuring benthic fluxes has previously been described80,81,82. Briefly, plots were divided into quarters and chamber bases (L50 × W50 × H15 cm) were positioned in a randomly chosen quarter ~10 cm from plot edges, and inserted 5 cm into the sediment. On day 2 (dark incubations), chambers were placed diagonally opposite to the day 1 position to minimise disturbance effects. HOBO Pendant temperature and light loggers (Onset) were installed in 16 of the chambers dispersed across the site, with an additional three secured on the seafloor (10 s sampling frequency). Domed Perspex lids were clamped onto bases on the incoming tide, encapsulating ~34 L of water. Lids were transparent for light incubations, whilst double-layered shade cloth covered lids for dark incubations. Previous measurements using HOBO loggers have recorded zero light inside chambers covered using this method (V. Rullens, unpublished data). Syringe-drawn water samples (60 mL) were collected in triplicate at the start and end of the ~4-h incubation. Ambient seawater samples (n = 3) were collected as chambers were sealed, and 3 light and dark pairs of 1 L bottles were filled and secured at the seafloor for the duration of the incubations; sampling the bottles at the end of incubations allowed determination of the contribution of water column processes to solute fluxes. Water column processes accounted for <7% of benthic solute fluxes in both light and dark conditions and were therefore ignored. Seawater DO was measured immediately using an optical probe (PreSens FIBOX 3 LCD trace v7); a two-point calibration was performed prior to measurements in a Na2SO4 O2-free (0%) solution and air-saturated water (100%) following the manufacturer’s instructions. Samples were then filtered through 0.8 µm glass fibre filters (Whatman GF/F) and stored frozen, in the dark prior to analysis of dissolved nutrient concentrations.
Weather conditions varied substantially between days of benthic flux measurements; day 1 was sunny with little wind wave activity whereas day 2 was cloudy with intermittent rain and some wind wave activity. Although the cloudier conditions experienced on day 2 were irrelevant in terms of incident sunlight (day of dark incubations), mean water temperature inside chambers differed between day 1 (23 °C) and 2 (19 °C), which could have impacted solute fluxes.
Sediment cores were collected from within each plot to characterise sediment properties. Six small cores (2.6 cm diameter × 2 cm depth) were pooled per plot and stored frozen, in the dark for analysis of sediment grain size and indicators of MPB biomass (chlorophyll a (Chl a) and phaeopigments (phaeo)). Four medium cores (5 cm diameter × 7 cm depth) were collected and 0–2 cm and 2–5 cm sections were pooled for OC analysis at both depth intervals and CaCO3 content at 2–5 cm (depth of burial). Two large cores (13 cm diameter × 15 cm depth) for macrofaunal analysis were collected and sieved in situ over a 500 µm mesh, preserved in 70% isopropyl alcohol. Finally, porewater pH was measured in each plot using a digital field probe (Eutech pHTestr1, 2; accurate to ±0.2 pH units with a tip diameter of 3 mm) at ~2 cm depth following calibration using pH 4 and 7 standard solutions.
Sediment samples were thawed, homogenised and divided for analysis of sediment properties. Grain size samples (~10 g) were digested in 10% hydrogen peroxide to remove organic matter before measuring using a Malvern Mastersizer 2000 (particle size range 0.05–2000 µm). Sediment pigment samples (Chl a and phaeo) were processed using standard procedures83 and analysed on a Turner 10–AU fluorometer using an acidification step. Percent organic and CaCO3 contents were determined from 5 g dried sediment samples (100 °C until constant weight) according to standard loss on ignition (LOI) procedures for OC84 and CaCO385. Macrofauna samples were stained with Rose of Bengal and identified to lowest possible taxonomic level (usually species). Filtered water samples were thawed and analysed for dissolved inorganic nutrient species (ammonium (NH4+), nitrite (NO2−) and nitrate (NO3−)) using standard colorimetric and fluorometric techniques (Astoria 2 Pacific autoanalyser).
Dissolved oxygen and nutrient fluxes (µmol m−2 h−1) were calculated by subtracting the final concentration (µmol L−1) of the given solute from the initial concentration and standardising by the incubation duration (h), chamber water volume (L) and enclosed sediment surface area (m−2). These fluxes underpinned the quantification of key ecosystem functions: light chamber DO flux was equivalent to net PP (NPP) and dark chamber DO flux was equivalent to sediment oxygen consumption (SOC; a proxy for community metabolism), while fluxes of nitrogenous compounds indicated rates of nutrient cycling. Concentrations of NO2− and NO3− were frequently below detection limits and are thus combined and represented as NOx.
In all analyses, organic matter treatment (i.e. the quantity of organic matter initially added to plots) was used as the continuous independent variable against which responses were measured. Using organic matter treatment better represented the initial stress experienced by the benthic ecosystem, whereas OC (measured at the time of flux incubations) alternatively indicated the degree of organic matter degradation that had occurred since plot establishment, which may vary according to the natural heterogeneity of the environment.
To determine whether organic matter and CaCO3 treatments (incorporated at 5 cm sediment depth) had altered sediment characteristics as intended, OC (2–5 cm) and porewater pH were regressed against organic matter treatment, and a t-test was performed to detect differences in CaCO3 content (2–5 cm) between +CaCO3 and −CaCO3 plots. Simple linear regression identified significant (α < 0.05) responses of the macrofauna community and ecosystem functions to organic matter treatment (using Statistica v13).
To simultaneously account for the gradient in organic matter treatment and assess the effects of CaCO3 addition on sediment characteristics, macrofauna community and ecosystem functions, PERMANOVA (using PERMANOVA+, Primer V7) were performed based on Euclidean distances with CaCO3 treatment considered a fixed factor and organic matter treatment a continuous co-variable. Where a significant interaction (p(perm) <0.05) occurred −CaCO3 and +CaCO3 treatments were considered separately for subsequent analyses, in the absence of a significant interaction the treatments were pooled. As PERMANOVA obtains p-values through permutation and does not assume normality, response variables were untransformed. For constructing DistLM, predictor variables were normalised and highly correlated variables (Pearson’s r > 0.8) were identified; the variable explaining the lesser proportion of variance was excluded from model selection to avoid collinearity86. Full models used a backward elimination procedure with the corrected Akaike’s Information Criterion (AICc) and 9999 permutations to obtain the most parsimonious model87.
Upon acceptance of this manuscript, the data supporting the results will be archived in an appropriate public repository and the data DOI will be included at the end of the article.
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We sincerely thank the University of Waikato Benthic Ecology Team (D. Bell (technician), R. Gladstone-Gallagher, V. Rullens, S. Mangan, B. Monahan, G. Petersen, J. Cope and R. Koverman) for their assistance during field experiment setup and data collection, and R Gladstone-Gallagher and S. Hailes of NIWA for guidance during macrofauna species identification. Funding for TD’s PhD scholarship and AML’s time was provided by NIWA (Coasts and Oceans Research Programme 5, Managing Marine Ecosystems, COME1902). Field costs and CAP and AH’s time were supported by MBIE contract UOWX1602.
The authors declare no competing interests.
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Drylie, T.P., Needham, H.R., Lohrer, A.M. et al. Calcium carbonate alters the functional response of coastal sediments to eutrophication-induced acidification. Sci Rep 9, 12012 (2019) doi:10.1038/s41598-019-48549-8