domain: sde sdu

text:
Daheydrey Payandi-Rolland
email: dahedrey.payandirolland@hotmail.com

Liudmila S Shirokova

Paty Nakhle

Marawit Tesfa

Ahmed Abdou

Carole Causserand

Bruno Lartiges

Jean-Luc Rols

Frédéric Guerin

Pascale Benezeth

Dahédrey Payandi-Rolland

Frédéric Guérin

Pascale Bénézeth

Oleg S Pokrovsky

Hailiang Dong

D Payandi-Rolland

D Payandi

Aerobic release and biodegradation of dissolved organic matter from frozen peat: Effects

Keywords:

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Introduction

Permafrost wetlands that store a large amount of carbon (C) in Arctic regions are severely affected by the ongoing global warming, which is referred to as the "Arctic amplification" [START_REF] Overland | When will the summer Arctic be nearly sea ice free?[END_REF][START_REF] Serreze | The emergence of surface-based Arctic amplification[END_REF]. Climate scenarios in Arctic regions predict that air temperature will increase by 2 to 4.9 °C before the end of the century (Raftery et al., 2017). This will increase the active layer thickness (ALT) and enhance soil subsidences and abrupt thermokarst events [START_REF] Grosse | Vulnerability and feedbacks of permafrost to climate change[END_REF][START_REF] Turetsky | Permafrost collapse is accelerating carbon release[END_REF]. As a consequence, a substantial amount of previously sequestered organic matter (OM, about 1330-1580 Pg-C) trapped in the permafrost [START_REF] Hugelius | Estimated stocks of circumpolar permafrost carbon with quantified uncertainty ranges and identified data gaps[END_REF][START_REF] Schuur | Climate change and the permafrost carbon feedback[END_REF] might be mobilised and reinjected into the global C cycle. The microbially-driven degradation of the released OM in the active layer or in thaw (thermokarst) lakes, generated by the soil surface subsidence can also be strongly affected by rising temperatures due to climate warming [START_REF] Grosse | Vulnerability and feedbacks of permafrost to climate change[END_REF][START_REF] Kirpotin | Western Siberia wetlands as indicator and regulator of climate change on the global scale[END_REF][START_REF] Kokelj | Advances in thermokarst research[END_REF][START_REF] Shirokova | Heterotrophic bacterio-plankton in thawed lakes of the northern part of Western Siberia controls the CO 2 flux to the atmosphere[END_REF].

Permafrost thaw occurs mostly in Arctic regions, mainly where soil temperature fluctuates around 0 °C [START_REF] Romanovsky | Permafrost thermal state in the polar Northern Hemisphere during the international polar year 2007-2009: a synthesis[END_REF] and where the permafrost is discontinuous to sporadic. Boreal and subarctic peatlands occupy large regions with significant soil C stocks in the form of frozen and thawing peat, namely in the Western Siberia Lowland (WSL, 1,300,000 km 2 ), North-Eastern European Tundra (300,000 km 2 ), Canada (1,240,000 km 2 ; with the Hudson Bay Lowland accounting for 372,000 km 2 ; [START_REF] Packalen | Carbon storage and potential methane production in the Hudson Bay Lowlands since mid-Holocene peat initiation[END_REF], USA (625,000 km 2 ), Finland (96,000 km 2 ) and Sweden (70,000 km 2 ) [START_REF] Gorham | Northern Peatlands: role in the carbon cycle and probable responses to climatic warming[END_REF][START_REF] Kuhry | The postglacial development of boreal and subarctic peatlands[END_REF][START_REF] Vitt | Functional Characteristics and Indicators of Boreal Peatlands[END_REF]. These wetlands are subjected to highly pronounced degradation of frozen peat and massive permafrost thaw (Kokelj et al., 2017b(Kokelj et al., , 2017a;;[START_REF] Loiko | Abrupt permafrost collapse enhances organic carbon, CO2, nutrient and metal release into surface waters[END_REF][START_REF] Overland | When will the summer Arctic be nearly sea ice free?[END_REF][START_REF] Turetsky | Permafrost collapse is accelerating carbon release[END_REF]. For example, from 2000 to 2015, the average annual soil temperature of the North-Eastern European Tundra increased from -2 ± 1 °C to +1.5 ± 0.5 °C which produced sizeable increase in ALT and caused major soil subsidences [START_REF] Kaverin | Active layer thickness dynamics in the tundra permafrost-affected soils: a calm site study, the European North of Russia[END_REF]. It is worth noting that the Eastern European Arctic may be among the key northern regions from which positive and negative carbon-climate feedbacks are likely to arise in the future [START_REF] Ciais | Five decades of northern land carbon uptake revealed by the interhemispheric CO 2 gradient[END_REF]. The main mechanism that underpins such feedback is the microbial processing of DOM of peat (terrestrial) origin, as it has already been shown from various non-permafrost [START_REF] Berggren | Efficient aquatic bacterial metabolism of dissolved low-molecular-weight compounds from terrestrial sources[END_REF] and permafrost [START_REF] Drake | Ancient low-molecular-weight organic acids in permafrost fuel rapid carbon dioxide production upon thaw[END_REF][START_REF] Mann | Utilization of ancient permafrost carbon in headwaters of Arctic fluvial networks[END_REF] settings. Since the DOM processed by the microbial community in surface waters can be released to the atmosphere as carbon dioxide and methane, it is important to better understand the pathways of these processes to predict their impact on the climate.

The main objective of this study was to evaluate the impacts of temperature and heterotrophic bacteria on C release and DOM biodegradation, using both the frozen peat and its aqueous leachate. We hypothesised an enhanced release of DOM from peat and its biodegradation due to an acceleration of heterotrophic bacteria metabolism with increasing temperature. Usually, both aerobic and anaerobic incubations are used to assess the biodegradability of permafrost soil materials (Heslop et al., 2019b;[START_REF] Knoblauch | Predicting long-term carbon mineralization and trace gas production from thawing permafrost of Northeast Siberia[END_REF][START_REF] Bracho | Temperature sensitivity of organic matter decomposition of permafrost-region soils during laboratory incubations[END_REF][START_REF] Treat | Temperature and peat type control CO2 and CH4 production in Alaskan permafrost peats[END_REF][START_REF] Waldrop | Molecular investigations into a globally important carbon pool: permafrost-protected carbon in Alaskan soils[END_REF] and a few microbiological studies of autochthonous bacterial communities in peat demonstrated that these communities are dominated by Alphaproteobacteria and Acidobacteria [START_REF] Ausec | Differences in the activity and bacterial community structure of drained grassland and forest peat soils[END_REF][START_REF] Basiliko | Controls on bacterial and archaeal community structure and greenhouse gas production in natural, mined, and restored Canadian peatlands[END_REF][START_REF] Dedysh | Cultivating uncultured bacteria from Northern Wetlands: knowledge gained and remaining gaps[END_REF][START_REF] Dedysh | Phylogenetic analysis and in situ identification of bacteria community composition in an acidic sphagnum peat bog[END_REF][START_REF] Kraigher | Microbial activity and community structure in two drained fen soils in the Ljubljana Marsh[END_REF][START_REF] Pankratov | Bacterial populations and environmental factors controlling cellulose degradation in an acidic Sphagnum peat[END_REF]. However, in this work, we focused on aerobic incubation, because i) most surface waters of frozen peatlands and supra-permafrost waters interacting with soil peat are fully or partially oxygenated [START_REF] Loiko | Abrupt permafrost collapse enhances organic carbon, CO2, nutrient and metal release into surface waters[END_REF][START_REF] Manasypov | Seasonal dynamics of organic carbon and met als in thermokarst lakes from the discontinuous permafrost zone of western Siberia[END_REF][START_REF] Raudina | Permafrost thaw and climate warming may decrease the CO2, carbon, and metal concentration in peat soil waters of the Western Siberia Lowland[END_REF] and ii) the potential C emissions under aerobic conditions are higher than under anaerobic conditions [START_REF] Bracho | Temperature sensitivity of organic matter decomposition of permafrost-region soils during laboratory incubations[END_REF]. For these incubations, we selected cultivable heterotrophic species (Iodobacter sp.) extracted from thermokarst lakes in a discontinuous permafrost peatland area and known to occur in arctic lake sediments [START_REF] Shirokova | Impact of cyanobacterial associate and heterotrophic bacteria on dissolved organic carbon and metal in moss and peat leachate: application to permafrost thaw in aquatic environments[END_REF][START_REF] Su | Iodobacter limnosediminis sp. nov., isolated from Arctic lake sediment[END_REF]. The choice of this bacterium was also made to simulate the interaction between frozen peat and surface waters, in which aquatic bacteria rather than soil bacteria may dominate the processing of organic carbon.

Material and methods

Bacteria and substrate: origins and use

Heterotrophic bacteria (Iodobacter sp., CdM7, Proteobacterian, Betaproteobacteria) were isolated from thermokarst lakes located in NE Europe permafrost-bearing peat bogs [START_REF] Shirokova | Impact of cyanobacterial associate and heterotrophic bacteria on dissolved organic carbon and metal in moss and peat leachate: application to permafrost thaw in aquatic environments[END_REF]. These aerobic gram-negative bacteria, rod-shaped cells (0.7 μm wide and 1.4 to 1.7 μm length) have one or several polar and lateral flagella. The bacteria were cultured to a stationary stage in a 10% nutrient broth (NB) on a shaker for 5 days at 25 °C in darkness. Prior to the addition of peat substrate, the heterotrophic bacteria were starved in 0.01 M NaCl for 3 days to remove internally and surface adsorbed nutrient resources [START_REF] Bundeleva | Experimental modeling of calcium carbonate precipitation by cyanobacterium Gloeocapsa sp[END_REF][START_REF] Bundeleva | Calcium carbonate precipitation by anoxygenic phototrophic bacteria[END_REF][START_REF] Shirokova | Impact of cyanobacterial associate and heterotrophic bacteria on dissolved organic carbon and metal in moss and peat leachate: application to permafrost thaw in aquatic environments[END_REF][START_REF] Shirokova | Effect of the heterotrophic bacterium Pseudomonas reactans on olivine dissolution kinetics and implications for CO2 storage in basalts[END_REF]. This treatment did not affect cell viability.

The frozen peat was collected at the edge of a thermokarst lake in the Bolshezemelskaya Tundra zone of NE Europe (discontinuous permafrost area, see [START_REF] Shirokova | Humic surface waters of frozen peat bogs (permafrost zone) are highly resistant to bio-and photodegradation[END_REF] for details), underneath the active layer (from 30 to 40 cm depth). The oligotrophic peat is 35% degraded and composed of Sphagnum angustifolium (20%), cotton-grass Eriophorum (25%), Scheuchzeria palustris (15%), bog-sedge Carex limosa (5%), lichens (5%), dwarf shrubs (5%) and some amount of wood debris (pine) and green mosses. The studied peat essentially made of Sphagnum is representative of boreal peatland ecosystems [START_REF] Turetsky | Trade-offs in resource allocation among moss species control decomposition in boreal peatlands[END_REF].

Two types of organic substrates were used for experiments: (1) solid frozen peat (SFP), sampled using a Russian peat corer (see details of sampling and handling in [START_REF] Morgalev | Bacteria primarily metabolize at the active layer/permafrost border in the peat core from a permafrost region in western Siberia[END_REF] and kept frozen until its use in the laboratory and (2) aqueous leachate of this frozen peat (FPL). The leachate was prepared via reacting the frozen peat with sterile MilliQ water (10 g dry L -1

), in aerobic conditions at room temperature under gentle mixing on a shaker. An initial DOC concentration between 12 and 20 mg L -1 was then reached, consistent with that occurring in natural thaw ponds and depressions of the permafrost zone (10-100 mg L -1 , [START_REF] Pokrovsky | Organic and organo-mineral colloids in discontinuous permafrost zone[END_REF][START_REF] Raudina | Permafrost thaw and climate warming may decrease the CO2, carbon, and metal concentration in peat soil waters of the Western Siberia Lowland[END_REF]. Note that, because the SFP contained its native microbial community, all incubations were run in the presence of this microbial community. After 3 days of reaction, the suspension was centrifuged at 4500g for 5 to 10 min, filtered through a 0.45 μm Nalgen sterile filter and then used as a substrate in experiments.

Experimental setup

Incubations

A scheme of the incubations setup is given in Fig. 1. A homogeneous suspension of the heterotrophic bacteria was transferred into 500 mL sterile bottles, with either solid peat (10 g dry L -1 in 300 mL of milliQ water) or aqueous peat leachate (300 mL), to obtain an initial bacterial biomass of 1 g wet L -1

. Reactors of substrate with and without added heterotrophic bacteria were placed at 4, 25 or 45 °C under aerated conditions (the aeration was achieved via Biosilico® porous stoppers) in a thermostated ping-pong shaker (25 and 45 °C), or on a ping-pong shaker placed in the dark inside a refrigerator (4 °C). The three chosen temperatures correspond to currently observed conditions: (i) at the beginning of spring and end of autumn (4 °C, [START_REF] Manasypov | Seasonal dynamics of organic carbon and met als in thermokarst lakes from the discontinuous permafrost zone of western Siberia[END_REF], (ii) in thermokarst lakes waters during summer (25 °C, [START_REF] Shirokova | Humic surface waters of frozen peat bogs (permafrost zone) are highly resistant to bio-and photodegradation[END_REF][START_REF] Pokrovsky | Impact of western Siberia heat wave 2012 on greenhouse gases and trace metal concentration in thaw lakes of discontinuous permafrost zone[END_REF] and (iii) 45 °C, a temperature that can be reached on the surface of moss and lichen cover during summer heatwaves (i.e. [START_REF] Pokrovsky | Impact of western Siberia heat wave 2012 on greenhouse gases and trace metal concentration in thaw lakes of discontinuous permafrost zone[END_REF]. The last case was used to reproduce possible maximum short-term summer temperatures expected in the case of most extreme scenarios of water or soil local heating. The control experiments were 0.45 μm-filtered frozen peat leachate, or frozen peat with MilliQ water, without the addition of Iodobacter sp. They were incubated under the same conditions as the experiments with added heterotrophic bacteria. As mentioned before, frozen peat comes with native microbial community, therefore in non-added heterotrophic bacteria experiments, the controls represented the activity of native microbial community associated with the peat substrates (SFP or FPL).

Sampling and chemical analyses

The SFP and FPL experiments lasted for 29 and 16 days, respectively, i.e. the time necessary to reach a steady-state concentration of DOC in the system. All the analyses performed on each sample during incubation are presented in Fig. 1. A homogeneous 15 mL suspension was sampled from each experimental reactor. A small non-filtered aliquot of the sample was used to measure pH (uncertainty of ±0.01 pH units) and specific conductivity (±0.1 μS cm -1

). The rest of the 15 mL sample was centrifuged at 4500g for 15 min and the supernatant was then filtered through a 0.45 μm filter (Minisart® syringe filter). In the experimental filtrates, the DOC was measured with a Shimadzu TOC-VSCN with an incertitude of 3%. The UV-absorbance of water samples at 254 nm was measured using a 10 mm quartz cuvette on a Spec-troFlex spectrophotometer (series 6600 -WTW), as this wavelength has been defined as the best proxy for surface water DOC [START_REF] Edzwald | Surrogate parameters for monitoring organic matter and THM precursors[END_REF][START_REF] Peacock | UV-visible absorbance spectroscopy as a proxy for peatland dissolved organic carbon (DOC) quantity and quality: considerations on wavelength and absorbance degradation[END_REF]. In addition, the specific UV absorbance (SUVA 254 , L mg C -1 m -1

) was used to assess the aromaticity of samples and the source of DOM. In the case of SFP experiment, additional analyses were conducted, such as organic acids and anions analyses, measured with a high-performance ion chromatography (Dionex ICS-5000+, analytical column: AS11-HC 4 μm).

Microbiological analyses

To evaluate the number of living bacteria (CFU, cells mL -1 ) in both SFP and FPL experiments, 1 mL of non-filtrated aliquots were inoculated in nutrient agar (2.8%) after serial dilution. Inoculated agars were placed in the dark for 5 days before visual counting.

In the case of SFP experiment, at the beginning and at the end of incubation (29 days), a duplicate of 12 mL aliquot per experiment at each temperature was collected to analyse the functional diversity of the bacterial community, using an EcoPlates® (Biolog Inc., Hayward, CA). The list of tested substrates (31 in total) is provided in Supplementary information (Table S1). Each well of the plate was inoculated with 130 μL of 1.2 μm-filtered (GF/C, Whatman) aliquot, and kept in the dark at 18 °C. After 5 days, the optical density of the plate at 590 nm was measured with a Synergy MX spectrophotometer (Biotek). The fol lowing calculated parameters were used to assess the change of microbial activity [START_REF] Gryta | The application of the biolog ecoplate approach in ecotoxicological evaluation of dairy sewage sludge[END_REF][START_REF] Stefanowicz | The biolog plates technique as a tool in ecological studies of microbial communities[END_REF][START_REF] Weber | One-dimensional metric for tracking bacterial community divergence using sole carbon source utilization patterns[END_REF][START_REF] Zak | Functional diversity of microbial communities: a quantitative approach[END_REF]: the average well colour development (AWCD, Eq. (1a)), the Shannon index of diversity (H, Eq. ( 1b)) defining the richness of the microbial community and the Shannon index of evenness (E, Eq. ( 1c)). In these equations, OD is the optical density of the well and p i is the proportional colour development of the well "i" over the total colour development of all wells of the plate.

(1a) (1b) (1c)

Transmission Electron Microscopy (TEM)

The peat particles in the SFP experiment were observed before incubation and after 29 days of incubation (using the solid phase obtained after centrifugation of the 15 ml aliquots) with a JEOL JEM-1400 HC transmission electron microscope (TEM) equipped with a Gatan Orius SC1000B CCD camera and after negative staining. Ultrathin sections were prepared as follows: at first, the samples were fixed with a 2.5% glutaraldehyde/2% paraformaldehyde in 0.1 M cacodylate buffer at ambient temperature for 2 h. The samples were then washed three times with the same cacodylate buffer and soaked during 1 h in 1% osmium tetroxide as a post-fixation step. The soaked samples were centrifuged for 5 min at 59g, the supernatant was removed, and the samples were embedded in agarose. The consolidated samples were placed in Eppendorf cones and dehydrated in ascending ethanol series (25, 50, 70 and 90% for 15 min and three times in 100% for 30 min). Their were then gradually infiltrated in epoxy resin (25, 50 and 75% for 1 h, and twice in 100% for 12 h) and polymerized at 60 °C for 48 h. 80 nm thick thin sections were cut from the resin-embedded samples with an ultramicrotome (Leica UCT), and placed on Formvar carbon-coated copper grids. Finally, the sections were stained with uranyl acetate and lead citrate.

Treatment of experimental results and statistics

In order to determine the concentration of biodegradable DOC (BDOC, Eq. ( 2)) over incubation time for the FPL experiments, the equation proposed by [START_REF] Vonk | Biodegradability of dissolved organic carbon in permafrost soils and aquatic systems: a meta-analysis[END_REF] was used:

(2)

where "t" is the incubation time in days. The apparent release (for SFP experiments) or removal (for FPL experiments) rate of DOC (R DOC, Eq. ( 3)) was calculated via the equation of a linear regression slope:

(3) where "t x " is the day of incubation at time "x" and "t mean " is the mean of incubation time in days. In addition, the apparent activation energy (Ea, Eq. ( 4)) was calculated from the Arrhenius equation (Arrhenius, 1889) using apparent rate of DOC release (in SFP experiments) or DOC removal (in FPL experiments) between temperatures (4 and 25 °C; 25 and 45 °C; and 4 and 45 °C) during the more active phase of DOC (i.e., during the first 2 days of incubation):

(4)

where "R" is the universal gas constant (R = 8.314 J K -1 mol -1

), "T 1 " and "T 2 " are the incubation temperatures in Kelvin and "R DOC(T″X″) " is the apparent release or removal rates of DOC at temperatures T 1 and T 2 .

Because the data were normally distributed, a statistical treatment, including the least square method for regression and the Pearson correlation, was used. A one-way ANOVA test was used to compare the trend in DOC and BDOC concentrations, R DOC rate, SUVA 254 , CFU, H, E and AWCD index between i) two temperatures, ii) added heterotrophic bacteria and control run and iii) at the beginning and at the end of experiments and assessed via the corresponding p values (Table S2). These treatments were performed under R software (version 3.5.2).

Results

The patterns of DOC and SUVA trend with time between 4 and 25 °C incubations in SFP and FPL experiments were insignificantly different (p values > 0.05; except for the SUVA 254 in SFP incubation). The FPL incubation results at 25 °C were not different than those at 45 °C (excepted for the BDOC, p values = 0.00146). However, the BDOC showed only slight differences between 4 and 25 °C (Table S2).

DOC behaviour

The changes in DOC concentrations in the SFP experiments over time exhibited similar trends at 4 and 25 °C with and without addition of Iodobacter sp.: after an initial increase by a factor of 2 to 5, from day 0 to day 12, the DOC concentration remained stable after 12 days (Fig. 2A andB). In contrast, at 45 °C, the DOC concentrations increased from 18.2 ± 2.4 at day 0 to 140.8 ± 1.9 mg L -1 at the last day of incubation in the SFP experiment with added heterotrophic bacteria, and from 11.9 ± 0.5 to 118.1 ± 3.9 mg L -1 in the control experiment (Fig. 2C). The apparent rate of DOC release in SFP experiments decreased with incubation time for all temperatures, with or without added heterotrophic bacteria (Table 1). For the 45 °C incubations, the R DOC between day 0 and 2 decreased from 17.7 ± 1.5 to 3.6 ± 0.12 mg L -1 d -1 in the presence of Iodobacter sp. and from 18.4 ± 0.66 to 3.2 ± 0.09 mg L -1 d -1 in the control experiment. Between 0 and 2 days of incubation at 4 °C, the apparent release rate of DOC was lower in Iodobacter sp. experiment compared to the controls (3.22 ± 0.79 mg L -1 d -1 versus 6.25 ± 1.25 mg L -1 d -1

). The trend of SUVA 254 over time in SFP incubations showed an initial increase followed by a stabilization after 2 days of exposure at all temperatures (around 5.0 ± 1.0 L mg C -1 m -1

), both for added heterotrophic bacteria and control experiments (Fig. 3A). The highest SUVA 254 value was observed at 25 °C at day 21 (6.4 ± 0.2 L mg C -1 m -1

). The temporal change of DOC in the FPL experiments was characterized by an approximately 2 mg L -1 decrease over the first 2 days, followed by a stabilization around 12 mg L -1 between day 2 to 16 in both added heterotrophic bacteria and control experiments at 4 and 25 °C (Fig. 2D andE). In the case of the 45 °C FPL experiment with added Iodobacter sp., the DOC increased after 10 days of incubation from 13.7 ± 0.16 to 18.5 ± 0.34 mg L -1 (Fig. 2F). In general, the BDOC was higher for control experiments than in the presence of Iodobacter sp. for the 25 and 45 °C incubations (Fig. 2H andI), but the opposite trend was observed at 4 °C of incubation (Fig. 2G). The BDOC at 4 and 25 °C sharply increased between days 0 and 2 (ca. 10-18%), then slightly decreased until day 5 and remained stable and positive until the last day of incubation. The incubations at 45 °C exhibited two clearly different patterns (Fig. 2I). While BDOC of control experiment was always positive and showed a 13% increase in values until day 9, followed by a 5.5% decrease between day 9 to 16, the added heterotrophic bacteria experiment showed negatives values (corresponding to DOC production/release) from day 0 to 16 with a 5-fold drop after day 9. The apparent rate of DOC removal in FPL incubations (Table 1) increased with incubation time at 4 and 25 °C without any significant difference between the two temperatures (p values = 0.497, Table S2). However, at 45 °C with added Iodobacter sp. there was a release rather than a removal of DOC in contrast with the control experiment at 45 °C, which revealed a net removal of DOC. The SUVA 254 trend in FPL experiments did not exhibit any clear trend with time, and the differ ences between added heterotrophic bacteria and control experiments, and between different temperatures, were not significant (Fig. 3B).

U N C O R R E C T E D P R O O F
U N C O R R E C T E D P R O O F D.
Apparent activation energies (Ea) of DOC release in the SFP incubations (R DOC ; Table S3) between 4 and 25 °C for the first two days of exposure showed a positive value with added heterotrophic bacteria (Ea added_bacteria(4-25) = 15.17 ± 3.9 kJ mol -1

) and a negative value in the control (Ea control(4-25) = -23.98 ± 0.5 kJ mol -1

). The Ea was positive between 25 and 45 °C (Ea added_bacte- ria(25-45) = 50.56 ± 18.1 kJ mol -1 but higher for the control Ea con- trol(25-45) = 72.56 ± 6.1 kJ mol -1 ). In the case of FPL incubations, the activation energy of DOC removal between 4 and 25 °C was low and negative in the added heterotrophic bacteria incubation (Ea added_bacte- ria(4-25) = -4.23 ± 12.3 kJ mol -1 ).

Organic acids and inorganic anions behaviour in SFP incubations

Among the measured anion (phosphate) and organic acids (acetate, formate, malate, oxalate and tartrate), only the phosphate concentration in the experiment with added Iodobacter sp. (Table 2) showed a significant increase in concentration over the time of incubation, following the order 45 °C ≥ 25 °C > 4 °C. The increase of PO 4 3-concentration from 0 to the 29th day of incubation was equal to 2.38 × 10 -2 , 2.24 × 10 -2 and 8.65 × 10 -3 mg L -1 d -1 at 45, 25 and 4 °C, respectively. In contrast, the control experiment only revealed a slight decrease of phosphate concentration over incubation time at all temperatures (-1.27 × 10 -3 , -1.32 × 10 -4 and -7.04 × 10 -4 mg L -1 d -1 at 4 °C, 25 °C and 45 °C, respectively).

Among the organic acids, only acetate exhibited a significant decrease in the control experiment (-4.89 × 10 -3 mg L -1 d -1 over 29 days of incubation at 4 °C), and a slight increase in the added Iodobacter sp. experiment (2.39 × 10 -4 , 3.19 × 10 -3 and 1.42 × 10 -3 mg L -1 d -1 at 4, 25 and 45 °C). The oxalate increased by 1.22 × 10 -2 mg L -1 d -1 at 45 °C in the added heterotrophic bacteria experiment. Formate, malate and tartrate did not exhibit any significant variation over the 29 days of incubations at all temperatures, and the changes of their concentrations did not generally exceed 10 -3 mg L -1 d -1 (0.05 mg L -1 from day 0 to day 29) which was <0.1% of the overall DOC level.

Bacterial cell number and Ecoplate analyses of microbial functional diversity in the SFP incubations

The live cell number in SFP (Fig. 4A) and FPL (Fig. 4B) experiments remained stable during incubations (around 10 9 CFU mL -1 with added Iodobacter sp. and 10 5 CFU mL -1 in the control). For experiments at 45 °C, the bacterial number drastically decreased between 0 and 2 days in SFP and FPL incubations, losing almost half of the initial cell number in both types of incubations. The incubation at 45 °C with SFP had CFU values comparable with those at 4 and 25 °C from day 20 to day 29. In contrast, the CFU values of FPL incubations at 45 °C were always an order of magnitude lower than those at 4 and 25 °C.

The AWCD parameter, reflecting the heterotrophic microbial diversity, was three times higher at the beginning of incubation in control experiments compared with added Iodobacter sp. experiments for all incubation temperatures (p value < 0.001, Tables 2 andS2). At the end of incubations (day 29), the AWCD with added Iodobacter sp. and control experiments were similar (p = 0.632, Table S2) for the three temperatures. A net decrease in richness (H) and evenness (E) of metabolic diversity was also detected for both control and added Iodobacter sp. experiments at all temperatures, except for the E index with added Iodobacter sp. at 4 and 25 °C (Table 2).

Ecoplate analyses also revealed a drastic decrease (i.e. ≥70%) of community richness, over 29 days of incubation for each type of consumed substrate (polymers, carbohydrates, amino acids, amines/amides and carboxylic acids, Fig. 5). In control experiments, the decrease of each substrate richness was >90% (hatched columns in Fig. 5), while for added Iodobacter sp. experiments, the decrease was between 70 and 80% at 4 and 25 °C and over 90% at 45 °C. Furthermore, for all types of incubations and at all temperatures, the polymers, carbohydrates, amino acids, and carboxylic acids were mostly consumed at the beginning of experiments, while at the end of experiments, only polymers and carbohydrates were used by the microbial community.

TEM observations of incubated peat

The TEM observations of peat at the beginning of the SFP experiments revealed a compact and complex material in which the original structures of the flora composing the peat are partially erased (Fig. 6A). However, some parts of the peat material still contain recognizable organelles such as the primary and secondary walls of vegetative cells, medium lamella, plasma membrane, inner cells residues and plasmodesmata, as illustrated in Fig. 6B.1, C.1 and D.1 and schematically outlined in Fig. 6B.2, C.2 and D.2. Cell walls seem to be well preserved figuring the double-wall configuration and sometimes even the plasma membrane (Fig. 6B, C andD), which appears as light matter under TEM. The cells of microorganisms were essentially observed near the inner part of the plant cells (Fig. 6B, D andC).

The TEM observations of peat incubated during 29 days showed that the inner part of the cells at 4 and 25 °C were substantially degraded compared with those after a 45 °C incubation (Fig. S1). Such change between different temperatures was detected for both added Iodobacter sp. experiments and their respective controls. The secondary walls seem to have been partially biodegraded, as it is demonstrated by lysis features of the walls in experiments with added Iodobacter sp. at 4 and 25 °C (Fig. 6D). It is worth noting that the number of living bacterial cells (CFU, cells mL -1 ) was lower in experiments at 45 °C compared with those carried out at 4 and 25 °C (Fig. 4A). Unfortunately, comparisons between incubations at different temperatures (i.e., assessment of the degree of the inner cell degradation and of the cell abundance) could not be statistically confirmed, first, because of an insufficient number of observations, and then, because spots of observation were too small to provide an appropriate representation of the intrinsic heterogeneity of the frozen peat.

U N C O R R E C T E D P R O O F D. Payandi-Rolland et al. Chemical Geology xxx (xxxx) xxx-xxx

Discussion

DOC trend during peat leaching and biodegradation

We hypothesised that the change of DOM through time in SFP incubation will be driven by ( 1) its release in solution from the peat and (2) its consumption by the microbial community. The release and the consumption of dissolved organic matter can be followed by the DOC trend in SFP incubations (Fig. 2A, B andC). In contrast, in FPL incubation (filtered substrates), we hypothesised that in the absence of particulate OM (POM), only biodegradation occurs and no DOM could be released (at the exception of lysis of microbial cells). In FPL experiment, the consumption of DOC (Fig. 2D, E andF) can be followed by the BDOC trend (Fig. 2G, H andI).

DOC release from frozen peat at different temperatures

The impact of temperature on the permafrost soil OM degradation has been intensively investigated, both in field soil heating experiments [START_REF] Eliasson | The response of heterotrophic CO2 flux to soil warming[END_REF][START_REF] Hartley | Effects of three years of soil warming and shading on the rate of soil respiration: substrate availability and not thermal acclimation mediates observed response[END_REF][START_REF] Melillo | Soil warming and carbon-cycle feedbacks to the climate system[END_REF] and in laboratory incubations [START_REF] Bracho | Temperature sensitivity of organic matter decomposition of permafrost-region soils during laboratory incubations[END_REF][START_REF] Mckenzie | Effect of temperature on production of CH4 and CO2 from Peat in a Natural and Flooded Boreal Forest Wetland[END_REF]. However, no strict consensus has been reached about the temperature control on soil OM degradation and significant controversies persist as discussed below.

In this work, no significant difference could be detected between 4 and 25 °C experiments in DOC concentration over time (Fig. 2A andB, p value : 0.199) and the apparent release rate of DOC (R DOC ) (Table 1, p value : 0.302). We then conclude, that under experimental conditions of this work, the temperature rise from 4 to 25 °C was not a key factor controlling OM release from peat of North-Eastern European Tundra. This is in agreement with results of Alaskan soil incubation in water (139 g soil +500 mL water) by [START_REF] Reyes | Rapid nutrient release from permafrost thaw in arctic aquatic ecosystems[END_REF], who demonstrated that the release of DOC and macronutrients (such as P, NO 3 -) were not affected by temperature changes from 7 to 17 °C for the active soil layer but were affected in the case of permafrost soils. The same observations were made using anaerobic incubations, by Heslop et al. (2019a) who demonstrated that the permafrost thaw affects the methanogen community composition and the temperature sensitivity of CH 4 production thus highlighting the higher temperature sensitivity of recently-thawed permafrost and seasonally-thawed active layer. Our observations also corroborate those of [START_REF] Ernakovich | Permafrost microbial community traits and functional diversity indicate low activity at in situ thaw temperatures[END_REF] who conducted experiments at 1, 10 and 20 °C and observed that the amount of OM used by microbes at these 3 temperatures were the same. Moreover, some studies even noticed an increase in the decomposition rate of OM at lower temperatures [START_REF] Del Grosso | Modeling soil CO2 emissions from ecosystems[END_REF][START_REF] Kirschbaum | The temperature dependence of soil organic matter decomposition, and the effect of global warming on soil organic C storage[END_REF][START_REF] Lloyd | On the temperature dependence of soil respiration[END_REF]. At the same time, a number of studies on permafrost peat biodegradation demonstrated an increase of OM decomposition with increasing temperature [START_REF] Davidson | Temperature sensitivity of soil carbon decomposition and feedbacks to climate change[END_REF][START_REF] Dioumaeva | Decomposition of peat from upland boreal forest: Temperature dependence and sources of respired carbon[END_REF][START_REF] Eliasson | The response of heterotrophic CO2 flux to soil warming[END_REF][START_REF] Friedlingstein | Climate-Carbon Cycle Feedback Analysis: results from the C4MIP Model Intercomparison[END_REF][START_REF] Hartley | Effects of three years of soil warming and shading on the rate of soil respiration: substrate availability and not thermal acclimation mediates observed response[END_REF][START_REF] Melillo | Soil warming and carbon-cycle feedbacks to the climate system[END_REF][START_REF] O'donnell | DOM composition and transformation in boreal forest soils: the effects of temperature and organic-horizon decomposition state[END_REF]. For ex et al., 2016). A similar pattern was observed in our incubations (i.e., a 3-fold increase in DOC concentration (Fig. 1C) and R DOC values (Table 1) at 45 °C compared to those at 4 and 25 °C). However, rare incubations studies were conducted at such high temperatures [START_REF] Shirokova | Impact of cyanobacterial associate and heterotrophic bacteria on dissolved organic carbon and metal in moss and peat leachate: application to permafrost thaw in aquatic environments[END_REF], limiting a possible comparison between the data. Note that the decomposition of recalcitrant soil organic matter exhibits a higher temperature sensitivity (Conant et al., 2008), which could explain the difference between the observed release rate of DOC at 4 and 25 °C compared with those at 45 °C. It is thus possible that the frozen peat used in our study releases only labile OC at 4 and 25 °C and that the excess of DOC observed at 45 °C corresponds to the recalcitrant OM of peat. It should be further noted that in our study, the substrate-normalized DOC yields of frozen peat (~5 mg g -1 peat) were substantially higher than the values obtained for organic soil samples of Alaska (0.14-2.2 mg g -1 of soil, [START_REF] Gao | Yields and characterization of dissolved organic matter from different aged soils in Northern Alaska[END_REF].

DOC removal during biodegradation of peat leachate

A former study of frozen peat leachate with the addition of Iodobacter sp. revealed no significant decrease of DOC at 4 °C but a slight decrease at 25 °C [START_REF] Shirokova | Impact of cyanobacterial associate and heterotrophic bacteria on dissolved organic carbon and metal in moss and peat leachate: application to permafrost thaw in aquatic environments[END_REF]. [START_REF] Oleinikova | Low biodegradability of dissolved organic matter and trace metals from subarctic waters[END_REF] reported a decrease in DOC concentration by 5 ± 3% over the first 96 h of incubation at 25 °C in a peat leachate. In contrast, the BDOC obtained in this study ranged between 15 and 20% after 2 days of incubation at 4 and 25 °C. These values are somewhat higher than the field incubation values of BDOC along the hydrological continuum of frozen peatlands (0 to 10%, [START_REF] Shirokova | Humic surface waters of frozen peat bogs (permafrost zone) are highly resistant to bio-and photodegradation[END_REF] but in agreement with those obtained for Arctic riverine BDOC (10 to 40%, [START_REF] Holmes | Lability of DOC transported by Alaskan rivers to the Arctic Ocean[END_REF][START_REF] Mann | Controls on the composition and lability of dissolved organic matter in Siberia's Kolyma River basin[END_REF][START_REF] Wickland | Biodegradability of dissolved organic carbon in the Yukon River and its tributaries: seasonality and importance of inorganic nitrogen: BIODEGRADABLE DOC IN THE YUKON RIVER[END_REF]. They are also consistent with the 10-40% range obtained for BDOC from the thawing and collapsing permafrost experiment of [START_REF] Abbott | Elevated dissolved organic carbon biodegradability from thawing and collapsing permafrost: permafrost carbon biodegradability[END_REF], as well as with values of the microbial utilisation of DOC in streams (3-11%) and in vegetation leachates (66%) of a 28 days incubations conducted at 20 °C [START_REF] Textor | Dissolved organic carbon turnover in permafrost-influenced watersheds of interior Alaska: molecular insights and the priming effect[END_REF]. In the case of incubation at 45 °C with added heterotrophic bacteria, we obtained negative BDOC values (Fig. 2I) which was not expected considering that the biodegradation was run in previously filtered solutions containing no particulate organic carbon. We hypothesize that some lysis of bacterial cells at these condi tions may be responsible for additional DOM production and apparently 'negative' BDOC values.

In our study, the biodegradation was followed for 16 days and showed stabilization of both DOC concentration (Fig. 2) and DOC removal (Table 1) between days 5 and 12 for the 4 and 25 °C experiments. This relatively short period appeared to be sufficient for the heterotrophic bacteria to remove the labile C by respiration [START_REF] Moran | Bacterial production on humic and nonhumic components of dissolved organic carbon[END_REF][START_REF] Søndergaard | A cross-system analysis of labile dissolved organic carbon[END_REF]. Consequently, the remaining C in FPL incubations (approximately 12 mg L -1

) represents the refractory C pool of the DOC. Although we hypothesised no release of DOC in FPL experiments, some studies have shown a bacterial contribution to DOC concentration in waters (30-50% in 0.7 μm filtrated freshwaters incubated at 20 °C) and have highlighted the resistance of this bacterially-derived organic matter to the microbial degradation [START_REF] Kawasaki | Bacterial contribution to dissolved organic matter in eutrophic Lake Kasumigaura, Japan[END_REF]. To a lesser extent, because of a smaller filtration pore size used in our study (i.e. 0.45 μm), the 12 mg L -1 of C remaining can also be partially composed of this bacterially-derived organic matter. The R DOC measured in this study in FPL experiments at 4 °C during the first two days of incubations (-1.18 ± 0.16 mg L -1 d -1 ; Table 1) is comparable with the values assessed in subarctic permafrost mire complex for the same incubation time (2 days) at 3 °C for the active layer where the consumption of DOC is about 1.75 ± 0.79 mg L -1 d -1 [START_REF] Roehm | Bioavailability of terrestrial organic carbon to lake bacteria: the case of a degrading subarctic permafrost mire complex[END_REF]. Furthermore, we did not detect any change in the apparent rate of DOC removal between 4 and 25 °C over this short incubation period which corroborates the former finding on very weak impact of temperature on labile C pool [START_REF] Biasi | Temperature-dependent shift from labile to recalcitrant carbon sources of arctic heterotrophs[END_REF][START_REF] Bracho | Temperature sensitivity of organic matter decomposition of permafrost-region soils during laboratory incubations[END_REF][START_REF] Conant | Experimental warming shows that decomposition temperature sensitivity increases with soil organic matter recalcitrance[END_REF][START_REF] Hartley | Substrate quality and the temperature sensitivity of soil organic matter decomposition[END_REF].

Heterotrophic bacteria functional diversity, microbial cell number and organic acids in the presence of frozen peat and frozen peat leachate

Consistent with the negligible impact of temperature on both DOC release from peat and DOC removal in peat leachate, the number of viable bacteria was similar at 4 and 25 °C ((10 ± 1) × 10 8 CFU mL -1

). This refutes the possibility of variance in the biodegradation rate as a function of temperature due to a difference in microbial cell numbers. In addition, the non-significant variations of richness (H), evenness (E) and AWCD indices between 4 and 25 °C incubations with SFP suggest a comparable metabolic activity of the microbial community at low and medium temperature. It indicates a quite high degradation rate of frozen peat from freshly thawed permafrost at 4 °C. This is contradictory to the hypothesis that the active microbial community at low temperature needs a few growing seasons to reach the degradation level of a warmer community after the first thaw of permafrost [START_REF] Ernakovich | Permafrost microbial community traits and functional diversity indicate low activity at in situ thaw temperatures[END_REF]. Furthermore, the lower values of AWCD, H and E indexes at 45 °C incubation compared with those at 4 and 25 °C are in agreement with observations made by [START_REF] Steinweg | Patterns of substrate utilization during long-term incubations at different temperatures[END_REF] showing that the microbial carbon use efficiency declined at the warmest temperatures.

U N C O R R E C T E D P R O O F
The exact reasons of this unusual temperature impact on microbial processing of DOC are unknown. Although the functional diversity of the microbial community was not affected by temperature, it is still possible that the community structure changed with temperature. Indeed, as it was shown for plant communities of peatlands, the taxonomic adaptation to climate change is not coupled with the functional diversity of community [START_REF] Robroek | Taxonomic and functional turnover are decoupled in European peat bogs[END_REF]. Further, Vigneron et Payandi-Rolland et al. Chemical Geology xxx (xxxx) xxx-xxx al. (2019) have shown a drastic difference in the microbial community of thermokarst lake between summer and winter driven by the change in redox environment. It follows that further metagenomic analyses of the microbial community structure are necessary to elucidate the mechanisms driving the temperature impact on biodegradation of DOM.

U N C O R R E C T E D P R O O F D.
Ecoplate analyses indicate that the AWCD as well as the Shannon index of richness and evenness (H and E) decrease over incubation time (except for E with added Iodobacter sp. experiment), reflecting a decrease of heterotrophic metabolic diversity, i.e., consumption of various nutritive resources by microorganisms. Soil DOM released from aged permafrost is known to contain a high proportion of biologically-labile protein-like substances [START_REF] Gao | Yields and characterization of dissolved organic matter from different aged soils in Northern Alaska[END_REF]. At the end of our experiment, carbohydrates and polymers were essentially consumed by microbial community (approximately 25 to 30%, respectively, of the total C used), which in the case of carbohydrates is slightly higher than the rate obtain by [START_REF] Boddy | Turnover of low molecular weight dissolved organic C (DOC) and microbial C exhibit different temperature sensitivities in Arctic tundra soils[END_REF] on the respiration of glucose and amino acids (<25% of the total respiration). This difference can be attributed to a larger microbial diversity of the frozen peat substrate used in the present study. Our peat sample originated just below the active layer, adjacent to the high bacterial metabolism zone [START_REF] Morgalev | Bacteria primarily metabolize at the active layer/permafrost border in the peat core from a permafrost region in western Siberia[END_REF], whereas the one used by [START_REF] Boddy | Turnover of low molecular weight dissolved organic C (DOC) and microbial C exhibit different temperature sensitivities in Arctic tundra soils[END_REF] was a topsoil sample (10 cm depth). This result suggests that the downward migration of the thawing front will intensify and diversify, on a short-term scale, the microbial activity of frozen peatlands. The higher metabolic capacity of this interface thus reflects a higher C mineralization potential by bacteria.

The frozen peat from the Bolshezemelskaya Tundra (BZT) released a relatively low amount of carboxylic acids and the DOC was generally refractory. This contrasted with the behaviour of ancient organic carbon from the Yedoma soils, in which about 53% of DOC was consumed over 200 h of incubation, with 87% of microbially consumed DOC being derived from acetate and butyrate respiration [START_REF] Drake | Ancient low-molecular-weight organic acids in permafrost fuel rapid carbon dioxide production upon thaw[END_REF]. Low concentrations of acetate (<2 μM) were reached in aqueous fluids that interacted with peat in the SFP experiments of the present study. These values are much lower than those reported in Yedoma permafrost cores from central Alaska, where acetate C accounted for 24% of DOC and ranged from 0.38 to 30 mM [START_REF] Ewing | Long-term anoxia and release of ancient, labile carbon upon thaw of Pleistocene permafrost: AGED ACETATE IN PLEISTOCENE PERMAFROST[END_REF]. This difference can be explained by the enrichment in acetate of the Yedoma samples under anoxic conditions (acetogenesis) in contrast to already partially processed peat used in this study (that still contained some labile C but very low acetate concentration) and that was incubated under oxygenated conditions.

Microscopic morphological features of reacted peat

General structure of peat

Until now, the TEM observations of frozen peat biodegradation have remained very limited and the majority of microscopic studies have been devoted to the characterisation of moss degradation [START_REF] Tsuneda | Modes of cell-wall degradation of Sphagnum fuscum by Acremonium cf. curvulum and Oidiodendron maius[END_REF]. Former scanning electron microscopy (SEM) observations reported similar well-defined features (plant cell walls and membranes) for the south Australian peat [START_REF] Dart | Peat culture of Rhizobium trifolii: an examination by electron microscopy[END_REF], although we observed a slightly more compact aspect of the frozen peat from Bolshezemelskaya Tundra (Fig. 6A). Such a compact structure of frozen peat from BZT is consistent with a general trend of decreasing the peat porosity and pore size with increasing depth [START_REF] Price | Importance of shrinkage and compression in determining water storage changes in peat: the case of a mined peatland[END_REF][START_REF] Rezanezhad | Structure of peat soils and implications for water storage, flow and solute transport: a review update for geochemists[END_REF].

The cell wall like fragments, identified in a previous study [START_REF] Dart | Peat culture of Rhizobium trifolii: an examination by electron microscopy[END_REF] can be compared to primary and secondary cell walls evidenced in this work (Fig. 6B, C andD). The inner cell residues which appear dark under TEM because of strong heavy metal staining are identified as the inner part cells residues (Fig. 6C, B andD). Most of those inner cell residues seem to have undergone intense degradation that might be linked to the activity of heterotrophic bacteria as described below.

Peat degradation features revealed by TEM

The peat used in this study was composed of plant cells components such as mosses (Sphagnum), lichens, dwarf shrubs and wood [START_REF] Manasypov | Experimental modeling of thaw lake water evolution in discontinuous permafrost zone: Role of peat, lichen leaching and ground fire[END_REF][START_REF] Shirokova | Impact of cyanobacterial associate and heterotrophic bacteria on dissolved organic carbon and metal in moss and peat leachate: application to permafrost thaw in aquatic environments[END_REF]. The TEM can be a useful tool in the investigation of peat biodegradation as it was used to monitor the degradation of wood [START_REF] Daniel | Use of electron microscopy for aiding our understanding of wood biodegradation[END_REF][START_REF] Daniel | Degradation of lignocellulosics by unique tunnel-forming bacteria[END_REF] and peat-forming sphagnum and other mosses structures [START_REF] Kettridge | Characterization of peat structure using X-ray computed tomography and its control on the ebullition of biogenic gas bubbles[END_REF][START_REF] Rezanezhad | Structure of peat soils and implications for water storage, flow and solute transport: a review update for geochemists[END_REF].

The poorly decomposed peat, like the one used in this study, is mostly represented by refractory compounds such as Sphagnum cell walls made of essentially cellulose but also of some non-cellulosic polysaccharides, including pectic polysaccharides as well as wood debris represented by lignitic components of cell walls of vascular plants ( [START_REF] Kremer | Distribution of cell wall components in Sphagnum hyaline cells and in liverwort and hornwort elaters[END_REF][START_REF] Steinen | Sugar proof in the cell walls of four cryptogams[END_REF][START_REF] Theander | Studies on sphagnum peat. III. A quantitative study on the carbohydrate constituents of sphagnum mosses and sphagnum peat[END_REF]. The hyaline cells of Sphagnum, whose major cell wall constituents are cellulosic, phenolic compounds, waxes, and polymerized lipids are very decay-resistant [START_REF] Aerts | Plant-mediated controls on nutrient cycling in temperate fens and bogs[END_REF][START_REF] Tsuneda | Modes of cell-wall degradation of Sphagnum fuscum by Acremonium cf. curvulum and Oidiodendron maius[END_REF][START_REF] Van Breemen | How Sphagnum bogs down other plants[END_REF]. They prevent the peat from microbial degradation as they form a barrier for microorganisms and their enzymes to gain access to cellulose [START_REF] Dobrovol'skaya | Analysis of ecological factors limiting the destruction of high-moor peat[END_REF][START_REF] Tsuneda | Modes of cell-wall degradation of Sphagnum fuscum by Acremonium cf. curvulum and Oidiodendron maius[END_REF]. For these reasons, only minimal alterations of peat structure and vegetative cells upon Iodobacter sp. interaction with frozen peat were detected in this study.

Osmium tetroxide used for the preparation of TEM sample is a heavy metal stain that provides contrasts in TEM images and reacts/cross-links with proteins and lipids, particularly phospholipids containing double bonds. In our study, the darker area under TEM appeared to be the inner part of cells, as it is strongly linked to the added metal stain [START_REF] Hayat | Basic Techniques for Transmission Electron Microscopy[END_REF]. We can also see that, over the incubation time, the concentration of dissolved phosphate increased by a factor of 5, 10 and 12, respectively at 4, 25 and 45 °C in all SFP experiments with added Iodobacter sp. (Table . 2). This can be explained by the degradation of these phosphate-rich areas that lead to the release of phosphate ions in the solution. Moreover, the lysis features of secondary walls observed at 4 and 25 °C may reflect the efficient degradation of complex components such as cellulose by Gram-negative bacteria [START_REF] Blanchette | Biological degradation of wood[END_REF][START_REF] Daniel | Use of electron microscopy for aiding our understanding of wood biodegradation[END_REF][START_REF] Eriksson | Microbial and Enzymatic Degradation of Wood and Wood Components[END_REF], occurring in the environment which is deficient in labile C compounds. Overall, the direct visualization of peat interaction with aqueous solutions and microbial cells complements the results of water chemistry monitoring thus providing new insights into the mechanisms of interaction between bacteria and organic matter.

Conclusion

The laboratory incubations performed in this study were aimed at quantifying several controlled parameters (primarily the temperature and one heterotrophic bacterium) which certainly cannot represent the wide heterogeneity of natural aquatic environments. In particular, this study does not take into account vertical and lateral water flow in soils, fresh input of OM, the use of POM by the microbial community, the diel change of temperature and respiration/photosynthesis cycle. However, the incubation of frozen peat and its aqueous leachate with and without culturable heterotrophic bacteria in a wide range of temperatures provided novel observations that might be necessary to consider in biogeochemical modelling of C cycle during permafrost thaw and surface water warming in permafrost zones of frozen peatlands. The unexpectedly high release of bio-available carbon from peat into lakes and fluvial systems, at the beginning and at the end of the active season (unfrozen), requires the consideration of the full active period for the estimate of C release into the environment. An important conclusion is that the major input of newly available OM from frozen peat to the aquatic ecosystems is likely to occur at the beginning of thermokarst lake formation in peat soil depressions, and this does not require particularly high summertime temperatures. (ii) The temporal change of functional diversity over the 4 weeks of incubation suggests that the downward migration of the thawing front (the interface between the active layer and the frozen peat) will intensify and diversify the microbial activity of frozen peatlands on a short-term scale. Overall, the high metabolic diversity observed in the native microbial community (originated from the frozen peat) incubations reflects a higher potential of C mineralization by the natural consortium, as compared to the added culturable heterotrophic bacteria. (iii) The morphological microscopic features of the association between bacteria and the peat particles were examined using TEM. Although the low number of observations and the high heterogeneity of the frozen peat used for the incubations do not allow any quantitative analysis, our study points out the preferential degradation of the inner plant cell by heterotrophic bacteria and the degradation of phospholipids materials leading to a release of phosphate.

Fig. 1 .

 1 Fig. 1. Schematics of frozen peat leachate (FPL; A) and solid frozen peat (SFP; B) leachate incubations with the various analyses performed on each sample.

Fig. 2 .

 2 Fig. 2. Dissolved Organic Carbon (DOC) of solid frozen peat (SFP, A, B and C) and frozen peat leachate (FPL, D, E and F), Biodegradable Dissolved Organic Carbon (% BDOC) of FPL (G, H and I) over incubation time at 4 °C (A, D and G), 25 °C (B, E and H) and 45 °C (C, F and I). These figures show the evolutionary trend of control incubations (dotted lines) and added heterotrophic bacteria incubations (solid lines). Note that the SFP and FPL experiments did not last the same duration. Most of the error bars are smaller than the symbol size. The negative BDOC in FPL experiments at 45 °C might be due to bacterial cell lysis and DOM production (see Section 4.1.2).

  Fig. 3. Temporal evolution of SUVA 254 during incubation of solid frozen peat (SFP; A) and frozen peat leachate (FPL; B). These figures show the evolutionary trend of control incubations (dotted lines) and added heterotrophic bacteria incubations (solid lines).

Fig. 4 .

 4 Fig. 4. Temporal evolution of CFU (log scale) during incubation of solid frozen peat (SFP; A) and frozen peat leachate (FPL; B). These figures show the evolutionary trend of control incubations (dotted lines) and added heterotrophic bacteria incubations (solid lines).

  Fig. 5. Percentage of richness (H) loss in solid frozen peat (SFP) experiment between day 0 and day 29 of incubation for each type of consumed substrates (hatched columns = controls, fill columns = with added heterotrophic bacteria, blue columns at 4 °C, green at 25 °C and red at 45 °C incubations). (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) ample, a 30 days incubation of moss and peat have shown that the increase of temperature from 5 to 20 °C increased the C release (DOC production) by 20 to 135% (O'Donnellet al., 2016). A similar pattern was observed in our incubations (i.e., a 3-fold increase in DOC concentration (Fig.1C) and R DOC values (Table1) at 45 °C compared to those at 4 and 25 °C). However, rare incubations studies were conducted at such high temperatures[START_REF] Shirokova | Impact of cyanobacterial associate and heterotrophic bacteria on dissolved organic carbon and metal in moss and peat leachate: application to permafrost thaw in aquatic environments[END_REF], limiting a possible comparison between the data. Note that the decomposition of recalcitrant soil organic matter exhibits a higher temperature sensitivity(Conant et al., 2008), which could explain the difference between the observed release rate of DOC at 4 and 25 °C compared with those at 45 °C. It is thus possible that the frozen peat used in our study releases only labile OC at 4 and 25 °C and that the excess of DOC observed at 45 °C corresponds to the recalcitrant OM of peat. It should be further noted that in our study, the substrate-normalized DOC yields of frozen peat (~5 mg g -1 peat) were substantially higher than the values obtained for organic soil samples of Alaska (0.14-2.2 mg g -1 of soil,[START_REF] Gao | Yields and characterization of dissolved organic matter from different aged soils in Northern Alaska[END_REF].

Fig. 6 .

 6 Fig. 6. TEM images of solid frozen peat (SFP) before incubation (A) and TEM images (B.1, C.1 and D.1) of SFP after 29 days of incubation at 25 °C (left panels). The right panels (B.2, C.2 and D.2) represent schematic interpretations of TEM images.

  (i) Peat lixiviation and peat leachate aerobic biodegradation under early spring and late autumn temperatures (surface water and soil fluids temperatures are 0 to 4 °C) release and consume amounts of organic carbon (OC) similar to those measured at 25 °C, i.e. a typi U N C O R R E C T E D P R O O F D. Payandi-Rolland et al. Chemical Geology xxx (xxxx) xxx-xxx cal summertime temperature in surface waters of frozen peatlands.

Table 1 R

 1

	4 °C			25 °C		45	°C
	Added bacteria	Control	Added bacteria	Control	Added bacteria	Control
	SFP incubations Day 0 to 2 Day 0 to 6 Day 0 to 12 Day 0 to 29 FPL incubations Day 0 to 2 Day 0 to 5 Day 0 to 12 Day 0 to 16	3.22 ± 0.79 3.82 ± 0.56 2.78 ± 0.49 1.51 ± 0.23 -1.18 ± 0.16 -0.22 ± 0.02 -0.04 ± 0.02 -0.03 ± 0.01	6.25 ± 1.25 3.78 ± 0.33 3.26 ± 1.29 1.56 ± 0.33 0.6 -0.08 -0.12 -0.07	5.28 ± 1.87 3.47 ± 0.38 2.14 ± 0.2 0.98 ± 0.07 -1.06 ± 0.24 -0.25 ± 0.29 -0.05 ± 0.06 -0.04 ± 0.07	3.01 ± 0.56 2.47 ± 0.1 1.71 ± 0.03 0.78 ± 0.06 -1.01 -0.29 -0.23 -0.19		17.74 ± 1.53 8.11 ± 0.25 5.88 ± 0.4 3.57 ± 0.12 0.19 ± 0.1 0.12 ± 0.01 0.17 ± 0.01 -0.26 ± 0.01	18.41 ± 0.66 9.05 ± 0.1 5.68 ± 0.53 3.18 ± 0.09 -0.48 -0.2 -0.12 -0.04

DOC : apparent release rate of DOC (mg L -1 d -1 ) for solid frozen peat (SFP) and apparent removal rate of DOC for frozen peat leachate (FPL) incubations, with and without added heterotrophic bacteria (control) at 4, 25 and 45 °C.

Table 2

 2 Ecoplate (AWCD, H and E), Anions and Organic acids analysis contents in solid frozen peat (SFP) incubations (control and with added heterotrophic bacteria) at the beginning and at the end of the experiments (day 0 and 29) and evolution rate of anions and organic acids concentration between day 0 and day 29.

	Control
			Incubation time (days)	0			29
			Temperature (°C)	4	25		45	4	25	45
	Ecoplate Anions and Organic acids	Concentration (mg L -1 ) Rate between day 0 and day 29 (mg L -1 d -1 )	AWCD Shannon richness index (H) Shannon evenness index (E) Phosphate (PO 4 3 -) Acetate Formate Malate Tartrate Oxalate Temperature (°C) Phosphate (PO 4 3 -) Acetate Formate Malate Tartrate Oxalate	1.044 268.5 ± 35.2 20.7 ± 1.3 0.095 0.52 0.035 0.035 0.018 0.045 -1.27 × 10 -03 1.044 268.5 ± 35.2 20.7 ± 1.3 0.016 0.014 0.034 0.011 0.017 0.015 4 -4.89 × 10 -03 6.28 × 10 -04 2.16 × 10 -05 1.53 × 10 -03 1.66 × 10 -03	1.044 268.5 ± 35.2 20.7 ± 1.3 0.11 0.027 0.008 0.015 0.018 0.016 25 -1.32 × 10 -04 0.061 14.4 ± 3 14.3 ± 1.6 0.032 0.092 0.048 0.028 0.072 0.096 -1.29 × 10 -02 -4.55 × 10 -04 3.59 × 10 -05 0 2.30 × 10 -04	0.085 19.6 ± 7.1 11.1 ± 2 0.009 0.055 0.009 0.006 0.017 0.017 -7.04 × 10 -04 0.093 18.9 ± 4.1 9 ± 3.4 0.029 0.09 0.018 0.009 0.019 0.035 45 8.93 × 10 -04 2.43 × 10 -04 8.64 × 10 -05 4.53 × 10 -05 -7.82 × 10 -04
	Expand Added heterotrophic bacteria
				Incubation time (days)	0		29
				Temperature (°C)	4	25	45	4	25	45
	Ecoplate Anions and Organic acids	Concentration (mg L -1 ) Rate between day 0 and day 29 (mg L -1 d -1 )	AWCD Shannon richness index (H) Shannon evenness index (E) Phosphate (PO 4 3 -) Acetate Formate Malate Tartrate Oxalate Temperature (°C) Phosphate (PO 4 3 -) Acetate	0.35 80 ± 4 12.6 ± 0.8 0.061 0.017 0.057 0.012 0.018 0.014 8.65 × 10 -03 0.284 64.5 ± 3.7 12.5 ± 0.7 0.066 0.012 0.007 0.008 0.017 0.013 4 2.39 × 10 -04	0.361 85.6 ± 8.2 13.5 ± 0.7 0.11 0.027 0.008 0.015 0.018 0.016 2.24 × 10 -02 0.08 17.4 ± 4.3 13.2 ± 2.7 0.334 0.05 0.011 0.008 0.017 0.015 25 3.19 × 10 -03	0.095 20.3 ± 5.4 12.2 ± 4.3 0.643 0.082 0.01 0.006 0.017 0.017 2.38 × 10 -02 0.03 7.1 ± 4.4 6.6 ± 5.4 1.302 0.099 0.013 0.009 0.021 0.421 45 1.42 × 10 -03

Acknowledgments

Dahédrey Payandi-Rolland was supported by a Ph. D. fellowship from the French "Ministère de l'Enseignement Supérieur, de la Recherche et de l'Innovation".

Paty Nakhle and Marawit Tesfa were supported by the "Axe transverse -AST GES" of the Observatoire Midi Pyrénées.

We thank Jessica Ferriol (EcoLab) for Ecoplates Biolog measurements, Frédéric Julien (EcoLab) for Dionex HPLC measurements and Vanessa Soldan (Meti) for her help with the TEM observations.

Declaration of competing interest

The authors declare that they have no known competing financial interests or personal relationships that could have appeared to influence the work reported in this paper.

Appendix A. Supplementary data

Supplementary data to this article can be found online at https://doi. org/10.1016/j.chemgeo.2019.119448.