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Sporadic hotspots for physico-chemical retention of aquatic organic carbon: from peatland headwater source to sea

Few studies have quantified the role of in-stream processes on net dissolved and particulate organic carbon (DOC and POC, respectively) export from peatland catchments, and those that have offer conflicting evidence. In this study, we evaluated evidence for active organic matter processing under field conditions, via a coordinated campaign across four UK catchments with peatland headwaters, targeted on potential ‘hotspots’ and ‘hot moments’ of physico-chemical carbon cycling. We hypothesised that specific hotspots and hot moments would occur where waters enriched with DOC and POC sourced from headwaters are exposed to: (1) mixing with freshwaters of different pH, conductivity and metal concentrations; and (2) mixing with seawater during autumn when DOC concentrations were at their highest. We observed instances of POC removal in headwaters, and potential for rapid conversion between dissolved and particulate carbon forms and for net removal of peat-derived carbon at confluences further downstream (where observed, on the order of 52–75 % for POC, and 5–44 % for DOC). Estuary transect surveys indicated that up to 30 % of fluvial DOC can be removed under high flow conditions. However, in the majority of cases concentrations remained within the range that would be expected based on conservative transport. These findings indicate that rapid (e.g. solubility-related) processes within the river system may be important but sporadic, thus are unlikely to provide major removal pathways for peat-derived organic carbon.


Introduction
Terrestrially-derived dissolved organic carbon (DOC) comprises the bulk of fluvial carbon (C) export in most peat-dominated upland headwaters in the UK (typically 87-93 % of total fluvial C; Billett et al. 2006;Dawson et al. 2004). The remaining components of fluvial C export are particulate organic carbon (POC) and dissolved inorganic C (DIC) species: bicarbonate (HCO 3 -) carbonate (CO 3 2-) or gaseous CO 2 , depending on pH. Heavily eroded peatlands are significant contributors of POC to rivers and streams, and in degraded environments POC may be the main contributor to fluvial C export (Pawson et al. 2012). While dissolved gaseous C sourced from peaty soils is readily lost from the stream system to the atmosphere (Hope et al. 2001), the fate of organic forms of fluvial C is more complex and may have a significant climate forcing effect if processes within the water column convert POC and DOC to CO 2 .
DOC and POC are potential sources of energy to aquatic organisms, and may be consumed either in the water column (e.g. Bernhardt and McDowell 2008) or in stream beds or the hyporheic zone (Fiebig and Lock 1991). However, biotic organic matter cycling is strongly dependent on availability of nutrients such as nitrate (Taylor and Townsend 2010;Wickland et al. 2012) and sensitive to organic matter 'quality' (Mann et al. 2012). On an annual basis, 13-21 % of the DOC in the Yukon river and its tributaries was estimated to be biodegradable (Wickland et al. 2012). Biodegradability (as assessed in 28-day incubations) was greatest in winter when the ratio of DOC to concentrations of inorganic N was lowest, suggesting that the relative availability of N is an overriding control on biotic DOC processing (Wickland et al. 2012). Wickland et al. (2012) also found that the proportion of biodegradable DOC (%BDOC) was significantly related to DOC 'quality' as inferred by optical and fluorescence proxy measurements. In tributaries of the Kolyma basin that drains to the Arctic Ocean, Mann et al. (2012) found that biological removal of DOC was strongly and positively correlated with fresh plant-derived C and ammonium (NH 4 ? -N) concentrations and negatively correlated with low molecular weight fulvic-like C, assumed to be a more degraded fraction of the DOC pool. In peatland streams, nutrient levels are low, so biological processing may be slow relative to in-stream residence times. For catchments with varying proportions of peat cover in northern Finland, potential DOC biodegradation rates in laboratory incubations (nutrients were added to prevent nutrient limitation) ranged from 4.1 to 17.9 % (Hulatt et al. 2014) and averaged 8.89 % (Asmala et al. 2014a) during incubations lasting 55 and 39 days, respectively. In a batch experiment Stutter et al. (2013) found that similar to other northern rivers, a maximum 19 % of DOM isolated from a Scottish moorland stream was biodegradable during 41-days incubation, and that the proportion of DOM decomposed could be predicted by DOM quality and 15 N content. Overall, these studies suggest that given time (on the order of days) and sufficient nutrients, biodegradation potentially removes up to 20 % of DOC from the water column in northern rivers.
DOC and POC may also be lost to bottom sediments through adsorption to mineral particles or flocculation (Sharp et al. 2006, McKnight et al. 2002), yet the potential for removal of fluvial C by such abiotic processes is poorly constrained and has generally received little attention. In a field experiment where DOC-rich waters were added to iron (Fe)-rich waters, fulvic acids were preferentially removed at a very rapid rate (of the order of milliseconds; McKnight et al. 2002). Adsorption and/or co-precipitation of DOC with Fe may therefore constitute a sink for DOC in upland waters, although re-suspension or dissolution may occur if conditions are favourable, and have been linked to seasonal variation in lake DOC concentrations in Esthwaite Water, Northern England (Hamilton- Taylor et al. 1996). Photo-mediated oxidation of aquatic DOC also potentially converts fluvial organic C to CO 2 , and is recognised as an important process in lakes (Anesio and Graneli 2004). There is experimental evidence that photo-oxidation may be important for Fe-rich and acidic streams (Molot et al. 2005;Wu et al. 2005), and recent work undertaken by Moody et al. (2013) suggests high rates of photo-mediated degradation of peat-derived organic matter.
Few studies have quantified the role of in-stream processes on net DOC and POC export from upland catchments, and those that have offer conflicting evidence. Some studies (Dawson et al. 2004;Temnerud et al. 2007) found little evidence of DOC processing, whilst other studies have suggested removal rates in the region of 10-20 % within small headwater catchments (Billett et al. 2006;Dawson et al. 2001), and higher rates in larger catchments (Algesten et al. 2004;Jonsson et al. 2007) and under field experimental conditions (up to 76 % decline in DOC; Moody et al. 2013). There have also been some studies providing evidence that DOC can be removed from the water column during water transit through the freshwaterseawater interface (Spencer et al. 2007;Uher et al. 2001), although once again other studies in different estuarine systems have concluded that DOC is fairly unreactive (Alvarez-Salgado and Miller 1998; Amon and Meon 2004). Sholkovitz et al. (1978) suggested that the humic acid component of DOC is most susceptible to flocculation, which could explain these differences. In support of this idea, Bowers et al. (2004) found a strong negative correlation between salinity and coloured dissolved organic matter (CDOM), as inferred by light absorbance at 440 nm wavelength, in an estuary and assumed to be of terrestrial plant origin. Recent experiments also have shown a change in dissolved organic matter (DOM) quality in river water treated with saline solutions. Kritzberg et al. (2014) found that high salinity caused a decrease in humic acids and aromatic DOM (as indicated by E4/E6 and SUVA 254 , respectively), and riverine average molecular weight has been observed to decrease even at low salinities (1-6; Asmala et al. 2014b). Similarly in freshwaters it is the hydrophobic component of humic and fulvic acids that is the most reactive (Sharp et al. 2006), and in coloured waters this fraction constitutes 60-80 % of the total DOC (Malcolm 1985), indicating significant potential for flocculation when DOC-rich waters enter estuaries. Evidence for POC removal in peat-influenced freshwater systems is limited, with estimates ranging from \5 to[50 % removal obtained from different studies (Dawson et al. 2004(Dawson et al. , 2012Worrall and Moody 2014). Pawson et al. (2012)  There are therefore various potential mechanisms for the removal of peat-derived DOC and POC from freshwaters, but 'hot spots' of biogeochemical cycling are most likely to occur when converging hydrological flowpaths deliver appropriate reactants to DOC-or POC-rich waters (McClain et al. 2003). Similarly, there may be occasions of rapid reactivity when waters are particularly enriched with DOC/POC ('hot moments'; sensu McClain et al. 2003). In upland peaty catchments, 'hot moments' of DOC delivery to streams have been observed to occur during late summer and autumn as a result of temperature-related production in soils and subsequent 'flushing' during high flow events (Chapman et al. 2010). Concentrations of POC in peaty headwaters also increase during high flow events (Pawson et al. 2008).
In light of the dearth of information and conflicting findings on the fate of peat-derived DOC and POC within river systems, the aim of this paper is to evaluate evidence for rapid, organic matter processing under field conditions, via a coordinated set of field measurements across four catchments targeted on potential 'hotspots' of physicochemical C cycling. We hypothesised that specific hotspots would occur where DOC-and POC-rich waters are exposed to: (1) mixing with river waters of different pH, conductivity, and metal concentrations; and (2) mixing with seawater during periods when delivery from headwaters is highest during autumn. The first hypothesis, affecting freshwaters, was addressed via synoptic survey of peatland river systems. Mixing of freshwater and seawater was addressed through transect sampling at an estuarine site.

Catchment site selection and sampling
Three peatland regions (and four catchments) in northern England and one in North wales were included in the study ( Fig. 1 and Table S1): The Tees catchment in the North Pennines; the Nidd catchment in the Central Pennines, the Etherow and Ashop catchments in the Peak District, and the Conwy catchment in North Wales. Within each study region, sites were selected to capture the change in physico-chemical conditions from peatland headwaters, through the transition from peaty to mineral soils further downstream. Samples were collected above and below confluences between streams (12 confluences in total) and from the upper and lower ends of nine linear river reaches, varying in length from approximately 0.4 km to over 2 km (Fig. 1). Stream waters in the four regions were sampled within 2 weeks of each other on three occasions (early March, late June/early July and late September/early October) in both 2011 and 2012. The majority of the sampling sites were ungauged for river flow, although flow data were available for some sites in the Tees and the Nidd regions. At all sites, sampling trips coincided with very low flow conditions in 2011 compared to 2012.

Estuary site selection and sampling
For the estuary study we focused on that of the Afon Conwy in North Wales. Compared to the Pennine river systems, the Conwy catchment is relatively small, with a large peatland area and little urban influence, so that a high proportion of organic matter entering the estuary is likely to be derived from peaty sources in the headwaters of the catchment. The site therefore provides a suitable location at which to evaluate the potential for processing of organic matter through the freshwater-seawater transition. The estuary itself is shallow, with a large tidal range, so that tidal volume exchange exceeds average river flows by a factor of 20 (Simpson et al. 2001). Around 10 km of the river are tidally influenced, providing the opportunity to sample across a long salinity gradient. A total of five estuary transect surveys were undertaken, in October 2010, March 2011, June 2011, September 2011 and September 2012 (the focus on autumn sampling reflected the relatively high inputs of peat-derived DOC that occur at this time). During each sampling trip, a boat was used to collect samples from mid-river, from freshwater through to seawater at the estuary mouth. With the exception of October 2010, all surveys were undertaken close to periods of peak tidal amplitude. Samples were collected at or close to high tide (for logistical reasons, as the boat could not be taken up-river at low tide) and a conductivity probe was used to identify sampling points spanning a full range of freshwater:seawater ratios. Consequently, samples were not necessarily collected at the same locations on each trip, although they extended across approximately the same length of river (about 15 km, from just downstream of the tidal limit to the estuary mouth).

Stream and estuarine chemistry
Stream temperature, pH and conductivity were measured in the field at the time of collection. All dissolved species were determined within a few days of collection on samples filtered through 0.45 lm nylon filters with the exception of POC. Total dissolved carbon (DC) and DIC were analysed by thermocatalytic oxidation (Analytik Jena Multi NC2100) and DOC determined as the difference Sporadic hotspots for physico-chemical retention of aquatic organic carbon: from peatland… 493 between DC and DIC. A certified reference material (QC WWW4A, VKI Reference Materials, Denmark) was used to verify DOC concentration and the precision of repeated analyses was within 5 % for DOC and 10 % for DIC. The anions chloride (Cl -), nitrate (NO 3 -) and sulphate (SO 4 2-) were determined by ion chromatography (Dionex ICS 3000 DC). Total dissolved metals and metalloids (Ca, Mg, Na, K, Al, Fe, Mn and Si) were determined by ICP-OES (Perkin Elmer 5300DV) and no assumption is made regarding charge. Dissolved inorganic nitrogen (DIN: NH 4 -N plus NO 3 -N) was determined colorimetrically (Skalar SAN?? continuous flow autoanalyser). Particulate organic carbon was determined from the mass of material retained on filtering through a pre-washed and pre-ashed 0.7 lm GF/F filter following combustion at 500°C to determine the organic fraction. Absorbance in the UV-visible range was measured by scanning spectrophotometer (Jacso V630) and the specific UV absorbance @254 nm divided by DOC concentration (SUVA 254 ) was used as an indicator of DOC aromaticity (Weishaar et al. 2003). Estuarine samples were analysed for conductivity, DOC, POC and UV-vis absorbance only. Method detection limits for DOC, DIC and POC were 1.3, 2.5 and 0.9 mg L -1 , respectively.

Stream data analysis
Changes in fluvial C concentrations and other chemical variables along reaches were calculated as the difference in concentration between downstream and upstream sites (such that a negative value indicates an apparent net loss or decrease in concentration at the downstream site). For each individual reach, differences across all sampling dates were tested for significance using Wilcoxon Signed-Ranks test.
For stream confluences, fluvial POC and DOC concentrations in confluence outflows were predicted using solute mixing models and/or flux models where discharge data were available (Nidd confluences; see below). The mixing models were developed using a suite of measured solute tracers (Cl -, SO 4 2? , Ca, K, Mg, Na and Si) to estimate the contribution to confluence outflow of each confluence inflow: = concentration of solute tracer in the inflows 1 and 2 and in the outflow, respectively. Solutes that were likely to show non-conservative behaviour in streams (DIN) or that are known to have a strong affinity with DOC (Fe, Al) were excluded from the model. This mixing model approach was applied to each tracer. The mixing ratio was calculated for each individual tracer and was rejected if the resulting model estimated a flow contribution for one inflow of more than 100 % or less than zero. If only two solutes remained after this step, both were used in the final model. If more than two solutes remained, the median of the remaining mixing ratios was calculated, and any single solute models that were more than 15 % different from the median on any date were also rejected (Schemel et al. 2006). All other solutes were retained and their median mixing ratios were used in the final model. This exercise was repeated for all confluences. In the Nidd catchment, stream flow was also measured at the time of sampling, either by salt dilution gauging (Nidd Reach 1/confluence 1) or continuous river flow gauging on a rated reach (Nidd Reach 2/confluence 2).
Instantaneous DOC, POC and DIC fluxes were calculated at the time of sampling as the product of measured concentration and discharge, and upstream C flux data were used to predict C fluxes downstream of confluences based on a conservative mixing model: where F I1 , F I2 are the instantaneous fluxes (mg s -1 ) of fluvial C in inflows (1, 2) upstream of the confluence; Q I1 , Q I2 are the stream flows (L s -1 ) of inflows (1, 2) at the time of sampling; C Oexp is the expected fluvial C concentration in the outflow assuming conservative mixing and no gain/ loss of water across the confluence. Along straight reaches, the instantaneous fluxes were used to estimate the expected minimum downstream concentration of fluvial C assuming no further inputs along the reach: where F 1 is the instantaneous flux (mg s -1 ) of fluvial C at the upstream start of the reach and Q 2 is the stream flow (mg L -1 ) at the downstream end of the reach at the time of sampling.

Estuarine data analysis
Data were analysed by plotting DOC and POC concentrations against lab-measured conductivity, as a proxy for salinity, i.e. sea-water content. If determinands follow a linear relationship with conductivity, this indicates conservative mixing as river water is diluted by seawater through the estuary (Spencer et al. 2007). A concave nonlinear relationship suggests net removal, whilst a convex non-linear relationship would suggest net production. To estimate deviation from a conservative mixing line, and thus the magnitude of any removal or production within the estuary, DOC and POC concentrations were linearly regressed against conductivity for all samples with conductivity higher than 20 mS cm -1 . This threshold was selected as a consistent (albeit arbitrary) cut-off, in order represent the seaward saline 'half' of the transect (the lowest conductivity value measured at the seaward end of a transect was 41 mS cm -1 ). In no case did we observe any clear evidence of non-conservative DOC or POC mixing above the 20 mS cm -1 threshold. The fitted line was then extrapolated back to the freshwater end of the transect and compared to actual measured concentrations. Absorbance at 254 nm (Abs 254 ) was included as a tracer for humic (i.e. peat or other terrestrially derived) DOC, as opposed to less coloured DOC (such as marine DOC) potentially present in the bulk DOC measurements.

Patterns of freshwater fluvial C by sample date and region
There was considerable variability in DOC concentrations and to a lesser extent POC concentrations both between sampling dates and across regions (Table 1). DOC concentrations were lowest during March 2011 and highest during summer 2012 coincident with low pH and conductivity. POC concentrations were often below detection limits during the March samplings in both years and highest during autumn. Both DOC and POC median concentrations, and median pH and conductivity, were lowest in the Conwy catchment, but there were no differences between other regions (Table 1). DIC was occasionally high at sites in the Nidd and Tees with calcareous geology, and low elsewhere. SUVA 254 values did not exhibit much variation between sampling dates or between regions. DIN concentrations were very low and frequently below detection limits, confirming the low nutrient status of these catchments.

Changes in freshwater fluvial C concentrations and fluxes across linear reaches
All forms of fluvial C exhibited some degree of concentration change along reaches, although for the most part these changes were small and statistically insignificant. In five out of the twelve reaches, differences between Sporadic hotspots for physico-chemical retention of aquatic organic carbon: from peatland… 495 Table 1 Median ( \DL below detection limits upstream and downstream fluvial C concentration were statistically significant, indicating a consistent pattern of C gain/loss across sampling dates (Table 2). Decreases in C were more frequent than gains, with the largest DOC declines occurring in Conwy reach 3 and Peak reaches one and three, and the largest POC decline occurring in Nidd reach 1. Across all sites and dates, changes in DOC and POC were positively correlated across reaches, and both were negatively correlated with changes in Mg and Si and positively with Fe (Table 3). Changes in POC were also negatively correlated with changes in pH and conductivity (Table 3).   Predicted concentrations were calculated assuming conservative mixing using either a solute mixing model or an instantaneous flux model (see ''Methods''). N = 6 (Conwy C2, C3; Nidd C2A; Peak C3); N = 5 (Nidd C2B; Peak C1, C2; Tees C2); N = 4 (Nidd C1; Tees C3). Negative values indicate observed concentrations were lower than predicted by solute mixing Sporadic hotspots for physico-chemical retention of aquatic organic carbon: from peatland… 497

Changes in concentrations and fluxes across confluences
Nine out of the twelve confluences met the criteria for mixing model selection. There were inconsistent results in the performance of mixing models for each confluence in predicting concentrations of solutes that were considered 'conservative' (Table 4). Large standard deviations reflect the variable performance between dates. The greatest differences between observed and predicted conservative solute concentrations occurred in the two Nidd catchments, and there was no clear difference between the performance of flow-based predictions and mixing-model prediction for Nidd C2. The most consistent model performance across sample dates (smallest variability) in terms of solute prediction occurred for the three Peak District confluences, Conwy C3 and Tees C2, where proportional flow contributions from the two inflows were fairly stable over time.
Both losses (predicted [ observed) and gains (predicted \ observed) in POC occurred at Peak, Nidd and Tees confluences (Fig. 2). Losses that were greater than the nominal cut-off (detection limit; 0.9 mg L -1 ) mostly occurred in the Peak District headwaters, C1 and C2, in March and July of both years (1.0-2.7 mg L -1 ; 52-75 %), and were accompanied by smaller increases in DOC concentration. A few relatively large apparent POC gains over expected values also occurred, and at one site (Peak C2; 3.0 mg L -1 ) was accompanied by an almost identical decrease in DOC (2.9 mg L -1 ). In contrast to POC, percentage DOC gains/losses relative to expected values were small ( Fig. 2; Table 4) but actual changes were similar in size to POC losses (1.7-2.9 mg L -1 ; 5-44 %) and gains (2.2-10.8 mg L -1 ; 6-136 %).

Changes in concentration in estuarine transects
Plots of DOC and POC versus conductivity (Fig. 3) show variable patterns of behaviour on different sampling trips. Freshwater inputs to the estuary had DOC concentrations ranging from 2.2-8.7 mg L -1 , with the highest concentrations observed in autumn surveys. DOC concentrations at the seaward end of the estuary varied from 1.6-4.3 mg L -1 , with the highest concentrations observed in September 2011. The net change in DOC from the freshwater to the seaward end of the transect ranged from -0.03 to -5.98 mg L -1 , and percentage changes from -1 to -68 % (Table 5). In all cases, a conservative mixing line fitted to the higher-salinity samples suggested dilution of DOC across the freshwater-seawater transition. However in most cases this mixing line did not coincide with the observed DOC concentration in the freshwater river. In the October 2010 survey, predicted freshwater concentrations were around 3.4 mg L -1 (38 %) lower than observed, suggesting significant net DOC removal through the estuary. In contrast, predicted concentrations for the other surveys exceeded observed concentrations by between 0.7 and 2.4 mg L -1 , suggesting some net DOC production. Absorbance at 254 nm (Abs 254 ) decreased more consistently and by a greater percentage than DOC (-81 to -97 %), leading to a decrease in SUVA 254 from values of 4.48 or higher at the freshwater end of the estuary to 1.55 or lower at the seaward end.
For POC, concentrations were consistently much higher (5.5-10.3 mg L -1 ) at the seaward end of the estuary than at the freshwater end (1-2.5 mg L -1 ), with percentage increases ranging from 120-930 %. For the October 2010 survey, observed POC concentrations through the estuary lay very close to a conservative mixing line, but in other surveys there was a large amount of deviation from the line, primarily towards the freshwater end of the estuary where large POC peaks were observed in the last three surveys. Despite this high variability across the salinity a b Fig. 2 Concentrations of fluvial C predicted assuming conservative mixing versus concentrations observed downstream of confluences. and POC (open diamonds; light grey dashed line) versus conductivity (as a measure of sea-water content) for five Conwy estuarine transect surveys. Linear regressions were fit to samples with conductivity [20 mS cm -1 (indicating transition to seawater). A linear relationship between DOC or POC and conductivity suggests conservative mixing; deviation from this line indicates nonconservative behaviour Sporadic hotspots for physico-chemical retention of aquatic organic carbon: from peatland… 499 gradient, observed POC concentrations at the freshwater end of the estuary did not deviate greatly from the value predicted from the conservative mixing line fitted to highsalinity samples.

Discussion
Fluvial C concentrations were dominated by DOC across all our sites, demonstrating that peaty headwaters are a potential source of energy to downstream aquatic communities. However the high DOC concentrations coupled with persistently low DIN concentrations suggest that these waters are not particularly favourable to biotic cycling. Furthermore, freshwater SUVA 254 values were similar across sample dates and regions, and are consistent with highly aromatic DOM from terrestrial inputs (Weishaar et al. 2003) as the main source of fluvial C in these catchments. In contrast, the variations in pH in rivers and conductivity in the estuary (and in rivers to a lesser extent) provide evidence that a range of chemical conditions existed between regions and sampling dates. Despite this, we did not find evidence for widespread consistent and rapid in-stream and estuarine processing of fluvial C. C losses were confined to a few biogeochemical 'hot spots' in the lower reaches of the catchment and sporadic elsewhere, yet where they occurred the losses were on occasion very high, up to 44 % for DOC loss downstream of confluences and approximately 30 % DOC loss during estuarinefreshwater mixing. These results provide evidence that peat-derived fluvial C may be highly reactive, and that rapid physico-chemical processes may at times cause losses that are significantly larger than reported at longer timescales for microbial consumption (Dawson et al. 2012;Hulatt et al. 2014;Stutter et al. 2013) or photochemical degradation (Mann et al. 2012;Worrall and Moody 2014). The strong negative correlation between reach-scale declines in DOC/POC and Mg and Si suggest that on most occasions apparent fluvial C losses are due to mixing with unmeasured sub-surface inputs of mineral-rich and POCor DOC-poor waters, rather than in-stream processing. However, the negative correlation of POC with pH and positive correlation with Fe may also indicate that at times conditions are favourable to flocculation and settling out of POC from the water column (McKnight et al. 2002;Sharp et al. 2006). For example, in October 2012, a very large decrease in POC (from 10.8 to 0.9 mg L -1 ) was observed in Nidd Reach 1 during moderately high flow. Parts of the Upper Nidd and Peak district catchments are actively eroding and similarly high POC concentrations have previously been observed, particularly during high flow events when POC may constitute up to 80 % of the organic C flux (Pawson et al. 2008). Not much is known about the reactivity and persistence of peat-derived POC in the river system. Dawson et al. (2012) found that less than 3 % of POC was biodegradable during an 18-hour incubation. Sudden loss over relatively short distances as observed in Nidd Reach 1 (less than 1 km), with an estimated residence time of less than 15 min, is unlikely to be due to biological processing. The most likely cause is gravitational settling as water moves through natural riffle and pool sequences. Adsorption to or flocculation with colloidal Fe would encourage removal by increasing the size and mass of particulates in a process similar to that used by water industries for removal of DOC (Sharp et al. 2006). This was one mechanism thought to remove both Fe and particulate organic matter in the Rio Negro/Solimões confluence in the Amzaon (Aucour et al. 2003). Certainly this could have contributed to the large loss of POC in Nidd reach 1 in October 2012 that was accompanied by a decrease in Fe (0.855-0.661 mg L -1 ) and an increase in pH from pH 4.4-5.7, which is within the optimal range for Fe-organic matter coagulation (Sharp et al. 2006). Based on discharge measurements taken at the time of sampling the estimated POC removal from the water column during this event equated to 468 mg C s -1 km -1 . This is an order of magnitude greater than maximum instantaneous C flux losses (DOC 15.5 mg C s -1 km -1 , DIC 6 mg C s -1 km -1 ) reported for a headwater stream in Scotland (Dawson et al. 2012). Gravitational settling of POC does not constitute a true loss from the system, however, and re-suspension and subsequent down-river transport cannot be ruled out.
At confluences, apparent POC losses were mainly observed in the Nidd and Peak District catchments, which had higher POC concentrations compared to the Conwy and Tees catchments. Large losses (and gains) in Nidd C1 have to be viewed with some caution because of the poor model performance for this site. The apparent losses at Peak District confluences were not accompanied by losses in metals, or by marked differences in pH between inflowing tributaries and therefore cannot readily be attributed to flocculation/precipitation. Alternative processes leading to POC loss could include gravitational settling during low flow conditions, conversion of POC to DOC and/or CO 2 , and removal by filter feeders (Monaghan et al. 2001). In July 2012, a POC gain (3.0 mg L -1 ) in Peak District C2 was accompanied by an almost equivalent DOC loss (2.9 mg L -1 ) suggesting that flocculation of DOC to POC had occurred. These observations are consistent with the concept that POC and DOC are dynamically linked, with conversion from one to the other occurring rapidly within streamwaters. Whereas any observed POC removals and gains occurred in the headwaters, occasional DOC losses were recorded at confluences further downstream (Conwy C2 and C3, Tees C3). These confluences were characterised by water sources draining quite different land areas (mixing of waters draining peats and mineral soils), suggesting that physico-chemical removal processes may also be important for DOC. At Conwy C3, for example, the Merddwr tributary is characterized by alkaline earth metal (median Ca 8.54 mg L -1 and Mg 2.09 mg L -1 ) and DIN concentrations (median 0.790 mg L -1 ) that were at least double those of the Conwy entering the confluence (median Ca 4.42 mg L -1 ; Mg 0.825 mg L -1 ; DIN 0.290 mg L -1 ). Coupled with the generally higher pH observed at downstream sites, these conditions could favour flocculation and/or microbiological consumption of DOC. In field incubations, Worrall and Moody (2014) observed an average DOC loss of just under 65 % over a 70-h period (less than 1 % per h), attributed to photo-oxidative and microbial consumption. Although not directly comparable to field experiments and observational studies, considerably smaller biodegradation losses have been reported for most laboratory incubations (e.g.\18 % in 55 days; Hulatt et al. 2014). The largest DOC loss at Conwy C3 (2.9 mg L -1 , 44 % of predicted) occurred under low flow conditions. With an estimated velocity of 1 m s -1 and a sampling distance of 670 m from the confluence, this gives a water residence time of 11-12 min and a DOC loss rate of 4 % per min. Whilst microbial and photo-oxidative loss cannot be ruled out in our study, large sporadic losses observed in the field suggest that on the time-scale (typically less than 1 h) of water mixing through the confluences and residing in linear reaches of 2-3 km, physicochemical removal processes are likely to be more important.
Results from the five estuary transects undertaken were variable. For DOC, there was clear evidence that terrestrially-derived DOC (much of which is likely to have been peat-derived under autumn high-flow conditions) was removed in the estuary during the October 2010 survey. This was not replicated during the remaining surveys, which suggested a small amount of DOC production within the estuary. However the much greater decreases in Abs 254 compared to DOC (and consequent large reductions in SUVA 254 ) along the estuarine transects indicate that terrestrially-derived DOC was being consistently and progressively replaced by DOC from other sources during mixing. These observations do not in themselves indicate non-conservative behaviour of terrestrial DOC, because it would be possible to reproduce these changes simply through mixing of two DOC end-members with contrasting SUVA 254 values. The pattern is, however, consistent with a gradual replacement of DOC from terrestrial sources with DOC from autochthonous sources towards the marine end of the estuary (Huguet et al. 2009). On all dates there was an increase in POC from mid-estuary towards the seaward end, suggesting an influence of phytoplankton which has been shown to be more bioavailable than terrestrial sources of DOC or POC (Sobczak et al. 2002). An analysis of Abs 254 against conductivity (data not shown) produced similar relationships to those for DOC concentration, with evidence of non-linear (i.e. non-conservative) change in the October 2010 survey, and linear (conservative) change in all subsequent surveys.
One contributing factor that may help to explain the lack of apparent DOC processing in the estuary (particularly during the March and June sampling trips) may be that terrestrial DOC inputs were too low to allow rapid withinestuary processing to be detected. Another factor is that rapid in situ mobilisation of POC from sediments, and short-term transitions between DOC and POC within the estuary, appeared to obscure the overall signal. Large peaks in POC during several surveys coincided with the 'estuarine turbidity maximum', the zone of freshwater-seawater mixing at the head of the rapidly rising tide where sediment re-suspension and biogeochemical processing are greatest (Spencer et al. 2007). As noted above, there is no clear evidence that these peaks were associated with either net production or net removal of POC, but it is possible that either concurrent DOC mobilisation, or the conversion of POC to DOC within the water column, contributed to slight apparent net estuarine DOC production in several of the surveys. A peak in DOC concentrations in the September 2011 survey, which occurred at higher salinity than the peak in POC, may be indicative of some POC to DOC conversion behind the head of the rising tide. These processes are likely to have been maximised by the higher turbulence associated with spring tide conditions when these surveys were undertaken.
In a hydrodynamic modelling study of the Conwy, Robins et al. (2014) have shown that water residence times within the estuary far exceed those within the freshwater catchment, due to the large volume of tidal flow compared to the freshwater input. Residence times increase when river flows are low, which can facilitate the 'trapping' of reactive solutes within the estuary. For DOC, however, our data suggest that estuarine processing of peat-derived DOC may be of greatest significance during autumn high flow events, because i) terrestrial inputs of DOC tend to be greatest at this time, and ii) shorter water residence times within the freshwater system limit the potential for photochemical or microbial breakdown of DOC before it reaches the estuary. This hypothesis is consistent with the results of Sholkovitz et al. (1978), who found that the humic acid component of DOC (which is largest in peat runoff) was strongly removed by flocculation during estuarine mixing, whereas the other constituents of DOC were largely unaffected. Consequently, it may only be during high-flow events that untransformed peat-derived DOC enters the estuary, where it is susceptible to flocculation and other removal processes. The untransformed DOC delivered by high flow events may also be relatively enriched in nutrients and therefore potentially more bioavailable (Asmala et al. 2014a). Additional high-flow estuary surveys would clearly be needed to confirm this interpretation and quantify the relative contributions of flocculation and microbial degradation to DOC loss. During low-flow events, however, our results are largely consistent with the results of Moody et al. (2013), suggesting that a high proportion of peat-derived DOC can be photo-degraded within the residence time of UK river systems. Similarly, observations from Sweden have shown a progressive shift from humic 'terrestrial' DOC to compositionally different 'aquatic' DOC during water residence in lakes (Kohler et al. 2013). Our results are also consistent with the previous work of Spencer et al. (2007) who found highest rates of estuarine DOC removal during high flow events, when inflow DOC concentrations and turbidity were highest.
For POC, terrestrial inputs to the estuary were so low that there appears to be little scope for further removal. The physical re-suspension and settling of sediments over tidal cycles within the estuary dominated our observations. Overall we found no evidence for either net removal or net gain of POC across the freshwater-seawater interface.

Conclusions
Some instances of apparent POC removal were observed in headwater streams, and rapid DOC removal was observed at some confluences further downstream, where peaty water mixes with less acidic and/or nutrient-rich runoff. The results suggest that there is potential for rapid conversion between particulate and dissolved carbon forms, and for net removal of peat-derived C in some circumstances (where observed, on the order of 52-75 % for POC in stream reaches, and 5-44 % for DOC at confluences).
Overall, however, there was no consistent pattern of DOC or POC removal across the study sites, and in the majority of cases concentrations remained within the range that would be expected for conservative transport. These findings indicate that rapid (e.g. solubility-related) processes within the river system are unlikely to provide major removal pathways for peat-derived organic carbon.
The limited number of estuary transect surveys do not allow definitive conclusions to be reached regarding the reactivity of peat-derived fluvial C across the freshwaterseawater transition, but results from one survey, supported by previous work, provide tentative evidence that substantial (circa 30 %) DOC removal can occur when high flow conditions transport relatively unmodified organic matter rapidly from the peatland to the estuary. The most likely fate of this DOC appears to be flocculation and precipitation to sediments within the estuary, but these sediments are highly dynamic in the estuary studied, and the permanence of this sink is thus uncertain.