Manon Bajard
email: manon.bajard@univ-smb.fr

Jérôme Poulenard

Pierre Sabatier

David Etienne

Francesco Ficetola

Wentao Chen

Ludovic Gielly

Pierre Taberle

Anne-Lise Develle

Pierre-Jérôme Rey

Pierre Taberlet

Bernard Moulin

Jacques-Louis De Beaulieu

Fabien Arnaud

M Vepraskas

Long-term changes in alpine pedogenetic processes: Effect of millennial agro-pastoralism activities (French-Italian Alps)

Keywords:

niveau recherche, publiés ou non, émanant des établissements d'enseignement et de recherche français ou étrangers, des laboratoires publics ou privés.

Introduction

Soils support multiple ecosystem services that are essential for life, such as food supply and water storage or for climate regulation, such as carbon sequestration (e.g., [START_REF] Daily | Ecosystem services supplied by soil[END_REF][START_REF] Adhikari | Linking soils to ecosystem servicesa global review[END_REF]. Because soils are a non-renewable resource over human time-scales [START_REF] Vanwalleghem | Impact of historical land use and soil management change on soil erosion and agricultural sustainability during the Anthropocene[END_REF], the potential of provided services can be threatened by human activities that trigger erosion and land degradation [START_REF] Oldeman | The Global Extent of Soil Degradation[END_REF][START_REF] Sabatier | Long-term relationships among pesticide applications, mobility, and soil erosion in a vineyard watershed[END_REF][START_REF] Vanwalleghem | Impact of historical land use and soil management change on soil erosion and agricultural sustainability during the Anthropocene[END_REF]. In Europe, the cost of soil degradation has been estimated to be 38 billion € per year [START_REF] Eu | Communication from the Commission to the Council, the European Parliament, the European Economic and Social Committee and the Committee of the Regions -Thematic Strategy for Soil Protection[END_REF]. The worldwide loss of carbon due to land use changes corresponds to more than one billion t•yr -1 since the 1960s (Le [START_REF] Quéré | Global carbon budget 2016[END_REF]. However, considering the lack of knowledge concerning soil functioning, no regulatory measures have yet been established to protect soils [START_REF] Puydarrieux | EFESE -Evaluation Française des Ecosystèmes et des Services Ecosystémiques -Rapport intermédiaire[END_REF]. This lack is related to the complexity of pedogenesis and the feedbacks between erosion, soil properties, vegetation and agricultural management [START_REF] Johnson | Evolution model of pedogenesis[END_REF][START_REF] Richter | Humanity's transformation of Earth's soil: Pedology's new frontier[END_REF][START_REF] Vanwalleghem | Impact of historical land use and soil management change on soil erosion and agricultural sustainability during the Anthropocene[END_REF], which have strongly varying response times.

Soils form slowly from the weathering of rocks and the incorporation of organic matter and are mixed and affected by vertical and horizontal transfers due to hydrological fluxes, bioturbation, slopes, etc. Soils thus depend on soil-forming factors defined by Jenny in 1941, namely, climate, organisms, relief, parent material and time. These factors were originally described for natural soil evolution.

The role of humans in soil evolution has long been neglected [START_REF] Yaalon | Framework for man-made soil changes-an outline of metapedogenesis[END_REF][START_REF] Richter | Humanity's transformation of Earth's soil: Pedology's new frontier[END_REF]. However, recent studies based on paleo-records that have yielded reconstructions of both soil evolution and human activities over long-term perspectives have demonstrated the importance of the human factor in pedogenesis [START_REF] Bajard | Progressive and regressive soil evolution phases in the Anthropocene[END_REF]. Metapedogenetic phases were introduced by [START_REF] Yaalon | Framework for man-made soil changes-an outline of metapedogenesis[END_REF] to define the changes in both pedogenetic processes and soil properties that are induced by humans.

Soil erosion must be considered within a long historical context in order to better understand the current drivers of soil degradation processes and their consequences for ecosystem functioning [START_REF] Trimble | The cow as a geomorphic agent-a critical review[END_REF][START_REF] Vanwalleghem | Impact of historical land use and soil management change on soil erosion and agricultural sustainability during the Anthropocene[END_REF].

During the last few decades, several studies have noted the potential of lake sediments to record physical erosion [START_REF] Giguet-Covex | Changes in erosion patterns during the Holocene in a currently treeless subalpine catchment inferred from lake sediment geochemistry (Lake Anterne, 2063 m a.s.l., NW French Alps): the role of climate and human activities[END_REF][START_REF] Simonneau | Holocene land-use evolution and associated soil erosion in the French Prealps inferred from Lake Paladru sediments and archaeological evidences[END_REF][START_REF] Sabatier | Long-term relationships among pesticide applications, mobility, and soil erosion in a vineyard watershed[END_REF][START_REF] Bajard | Erosion record in Lake La Thuile sediments (Prealps, France): evidence of montane landscape dynamics throughout the Holocene[END_REF][START_REF] Arnaud | Erosion under climate and human pressures: an alpine lake sediment perspective[END_REF], changes in the degree of soil weathering [START_REF] Dearing | Preliminary reconstruction of sediment-source linkages for the past 6000 yr at the Petit Lac d'Annecy, France, based on mineral magnetic data[END_REF][START_REF] Arnaud | Lake Bourget regional erosion patterns reconstruction reveals Holocene NW European Alps soil evolution and paleohydrology[END_REF][START_REF] Brisset | Non-reversible geosystem destabilisation at 4200 cal. BP: sedimentological, geochemical and botanical markers of soil erosion recorded in a Mediterranean alpine lake[END_REF][START_REF] Bajard | Progressive and regressive soil evolution phases in the Anthropocene[END_REF], pedogenetic processes [START_REF] Mourier | Contribution de l'approche sédimentologique à la reconstitution de l'histoire des sols[END_REF][START_REF] Mourier | Distinguishing subalpine soil types using extractible Al and Fe fractions and REE geochemistry[END_REF][START_REF] Giguet-Covex | Changes in erosion patterns during the Holocene in a currently treeless subalpine catchment inferred from lake sediment geochemistry (Lake Anterne, 2063 m a.s.l., NW French Alps): the role of climate and human activities[END_REF][START_REF] Malkiewicz | Holocene vegetation history and soil development reflected in the lake sediments of the Karkonosze Mountains (Poland)[END_REF][START_REF] Hošek | Late Glacial erosion and pedogenesis dynamics: evidence from high-resolution lacustrine archives and paleosols in south Bohemia (Czech Republic)[END_REF], and the progressive and regressive phases of pedogenesis [START_REF] Brisset | Non-reversible geosystem destabilisation at 4200 cal. BP: sedimentological, geochemical and botanical markers of soil erosion recorded in a Mediterranean alpine lake[END_REF][START_REF] Malkiewicz | Holocene vegetation history and soil development reflected in the lake sediments of the Karkonosze Mountains (Poland)[END_REF][START_REF] Bajard | Progressive and regressive soil evolution phases in the Anthropocene[END_REF]. Lakes sediments indeed store soil particles obtained from catchment fluxes and erosion triggered by human activities and/or climatic changes that correspond to soil development at the date of storage, providing a record of their evolution. Changes induced by erosion will depend on the characteristics of the soil profile, and thus into early pedogenetic processes. Few studies on soil evolution deciphered from lake sediments succeed in making accurate observations during the Anthropocene [START_REF] Mourier | Distinguishing subalpine soil types using extractible Al and Fe fractions and REE geochemistry[END_REF][START_REF] Giguet-Covex | Changes in erosion patterns during the Holocene in a currently treeless subalpine catchment inferred from lake sediment geochemistry (Lake Anterne, 2063 m a.s.l., NW French Alps): the role of climate and human activities[END_REF][START_REF] Malkiewicz | Holocene vegetation history and soil development reflected in the lake sediments of the Karkonosze Mountains (Poland)[END_REF] because, among other factors, catchments drain the soil landscape diversity [START_REF] Dreibrodt | Lake Belau and its catchment (northern Germany): a key archive of environmental history in northern central Europe since the onset of agriculture[END_REF]. It is necessary to understand the interdependence of landscape history (i.e., vegetation changes, human activities), soil evolution and erosion to sort the main forcing factors and their consequences on the agro-ecosystem to adapt its future management and ensure its sustainability.

Located in the Northwestern Alps, the Petit Saint-Bernard Pass area marks currently the border between France and Italy. Archaeological surveys and paleo-environmental studies enable the reconstruction of the landscape evolution and occupation phases around this pass. The oldest occupation phases were evident since the Neolithic period, and occurred mainly during the early Bronze period (ca. 4000 cal. yrs BP), the late Bronze period (3000 cal. yrs BP) and then in the Roman and Medieval periods [START_REF] Crogiez-Petrequin | Col du Petit Saint Bernard: Les fouilles du bâtiment ouest 2003-2005 Epoque Gallo-Romaine[END_REF][START_REF] Leveau | Le pastoralisme antique autour du col du Petit-Saint-Bernard. Alpis Graia[END_REF][START_REF] Miras | Dynamique des écosystèmes et impact de l'homme dans le secteur du col du Petit Saint Bernard au cours de l'Holocène[END_REF][START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF][START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF]. Paleosols and archaeological stratigraphy indicated different occupation phases and recurrences within different soil horizons. Thus, we have an ideal site where human activities are well-documented, to assess their effects on soil evolution. Pollen and subfossil chironomid analysis from seven peat bog records collected around the pass at elevations ranging from 1850 to 2345 m a.s.l., indicate that changes in the landscape and climate occurred throughout the Holocene [START_REF] Millet | Les assemblages de chironomidae et les cortèges polliniques, outils de reconstitutions quantitatives des changements du climat Holocène: une approche croisée au col du Petit Saint Bernard[END_REF][START_REF] Miras | Dynamique des écosystèmes et impact de l'homme dans le secteur du col du Petit Saint Bernard au cours de l'Holocène[END_REF], but do not permit characterization of the effects of human activities on soil erosion dynamics. In this context, we studied the sediments from the largest lake on the Italian side, Lake Verney, to reconstruct, past soil evolution and human activities throughout the Holocene, using multiproxy lake sediment archives and present-day soil analysis. Data derived from paleosols [START_REF] Moulin | Les séquences pédo-sédimentaires des versants du col du Petit Saint Bernard[END_REF][START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF], charcoals [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF] and archaeology (e.g., [START_REF] Rey | Occupations et circulations pré-romaines autour du Col du Petit-Saint-Bernard; méthode et premiers résultats d'une étude archéologique et sédimentaire de la montagne alpine[END_REF][START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF] then allowed us to validate and complete the Lake Verney sediment record and provide a complete soil evolution at the landscape scale. Finally, we integrated this evolution into the evolution cycle of the ecosystem.

Materials and methods

Study site

The Petit Saint Bernard Pass (2188 m a.s.l.) is located in the Western Alps, on the French-Italian border (Fig. 1-a), and it separates the villages of Séez in the Tarentaise valley (France) and La Thuile in the Aoste valley (Italy). On the Italian side of the pass, Lake Verney (2088 m a.s.l.) has a surface of 0.2 km 2 and a maximum depth of 21 m. The lake is fed by three main streams that flow from the south. Its catchment covers an area of 3.5 km 2 and rises up to 2900 m a.s.l. According to the weather observation network of the alpine massif (ROMMA), the mean temperatures at the pass range from -3.4 °C in winter to 9.7 °C in summer (these values represent averages for 2014-2016). Snow covers the area from November to June, and the lake is ice-covered during winter. The western part of the catchment is underlain by Jurassic calcareous schists (Lias) and black limestones (Dogger). The eastern side of the pass is characterized by sandstone and pelites of the Briançonnais Houillere zone (Fig. 1-c). There are currently no trees in the catchment. Around the lake, grazed grasslands are dominated by matgrass and thufurs and are punctuated with Vaccinium myrtillus and V. uliginosum and several wetlands (Fig. 1-b). The current upper tree line (mainly Picea abies) is situated at approximately 1950 m a.s.l. on both sides of the pass. Anthracological analysis indicated an upper tree line of Pinus cembra between 2300 and 2500 m before human clearing [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF]. Fire episodes were recorded regularly in soils, suggesting that pasture activities occurred continuously until the present. Several remains of pastures structures were identified, mainly for cattle farming, in addition to Roman buildings situated along the Roman road that crossed the pass [START_REF] Leveau | Le pastoralisme antique autour du col du Petit-Saint-Bernard. Alpis Graia[END_REF][START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF]. Surveys and pedo-sedimentary profiles performed on a 250-km 2 area covering both sides of the pass for archaeological analysis showed specific soil patterns above 1900 m, with mainly Stagnosols and sparse Podzols [START_REF] Moulin | Les séquences pédo-sédimentaires des versants du col du Petit Saint Bernard[END_REF][START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF].

Soil sampling

An archaeological and pedo-sedimentary survey was performed between 2003 and 2007 in the area of the Petit Saint-Bernard Pass [START_REF] Moulin | Les séquences pédo-sédimentaires des versants du col du Petit Saint Bernard[END_REF][START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF] within the framework of the Interreg III A 2003III A -2006 project. We used anew the 5 profiles from this earlier study that are closest to the pass (LTH/Lac Verney -Sondage 10, LTH/Le Verney Dessus -Sondage 2, Séez -Les Gouillons 13, Séez -Les Gouillons 15 and PSB7; the names of these profiles are simplified to PSB1, PSB2, PSB4 and PSB3, respectively) for soil analyses (Fig. 1-c). We sampled three new profiles on each side of the lake: VERS1, VERS2 and VERS3. PSB1 (2100 m a.s.l.) is located north of Lake Verney. PSB2 (2262 m a.s.l.) is located near Lake Verney Dessus, in the northern part of the Lake Verney catchment. VERS 1 and VERS 2 are located on either side of the lake; VERS3 is to the south of the lake. PSB7 is located on the flat area west of the pass on the Italian side. PSB4 and PSB3 (2000 m a.s.l.) are situated on the French side of the pass. Soil profiles were described with color, texture, structure and HCl effervescence test. The FAO (Food and Agriculture Organization) soil classification (WRB -FAO, 2014) and the Guidelines for soil description (FAO, 2006) were used for horizon and soil denominations. At least one sample was collected per horizons and sieved to 2 mm for further laboratory analyses.

Sediment sequence and chronology

Coring

Two coring missions were undertaken to retrieve sediments from the lake Verney in autumn 2012 and winter 2013. Short gravity cores were taken in 2012 from a small boat, and three longer sections (VER13-01, 02 and 03) that are approximately 2.4 m each in length were retrieved in 2013 from the ice-covered surface of northern flat part of the lake (45°41′19.8″N, 6°52′57.06″E) at a depth of 15 m using an Uwitec piston coring device. The deepest part of the lake was avoided regard to rock landslides south of the lake. The cores were split into two halves. Each half was described in detail, and pictures were taken with a 20-pixel•mm -1 resolution. The lithological description of the cores allowed the identification of different sedimentary units. A composite profile VER13-I was built using XRF-correlation from the three sediment sections obtained during the 2013 coring mission (the IGSN codes IEFRA05GT, IEFRA05GU and IEFRA05GV correspond to VER13-01, VER13-02 and VER13-03, respectively; IGSN codes refer to an open international database, www.geosamples.org). Data from a short gravity core (VER12-P4) obtained in 2012 (IGSN code: IEFRA00BU) were included to provide a well-preserved water-sediment interface.

XRF core scanner

The relative contents of major elements were analyzed by X-ray fluorescence (XRF) at high resolution (1 mm sampling step) on the surface of the sediment core with an Avaatech Core Scanner (EDYTEM Laboratory, CNRS-Université Savoie Mont-Blanc). The X-ray beam was generated with a rhodium anode and a 125-μm beryllium window, which allows a voltage range of 7-50 kV and a current range of 0-2 mA. The split core surface was first covered with a 4-μm-thick Ultralene film to avoid contamination and desiccation of the sediment. The element intensities were expressed in counts per second (cps). The geochemical data were obtained with different settings according to the elements analyzed. These settings were adjusted to 10 kV and 2 mA for 20 s to detect Si, Ca, Al, Fe, Ti, K, Mn, and S. For heavier elements (i.e., Sr, Rb, Zr, Br, and Pb), measurements were performed at 30 kV and 1.2 mA for 80 s.

Grain-size distribution

The grain-size distribution of the sediment was determined at high resolution, every 1 cm, using a Malvern Mastersizer 2000G laser particle sizer. Ultrasonics were used to dissociate mineral particles and to avoid their flocculation. Results of the grain-size distribution were processed with MATLAB software and presented as a contour plot with a color scale according to the percentage abundance of particles for each grain-size class.

Sedimentary environmental DNA (sedDNA)

To reconstruct past vegetation and the nature of herds (i.e., cows or sheep) by DNA analysis, we sampled 55 slices of 2.5 to 3-cm thickness covering the whole sediment core, following the strict laboratory precautions described in [START_REF] Giguet-Covex | Long livestock farming history and human landscape shaping revealed by lake sediment DNA[END_REF]. For each sediment slice, we mixed 15 g of sediment with 15 ml of saturated phosphate buffer (Na2HPO4; 0.12 M; pH ≈ 8) for 15 min. The mixture was then centrifuged (10 min at 10,000 g). 12 ml of the resulting supernatant were transferred to Amicon® Ultra-15 10 K Centrifugal Filter Devices (Millipore) and centrifuged (20 min at 4000 g) for sedDNA concentration. 400 μl of the resulting concentrate was kept as starting material for DNA extraction using the NucleoSpin® Soil kit (Macherey-Nagel) [START_REF] Stucki | Soil sampling and isolation of extracellular DNA from large amount of starting material suitable for metabarcoding studies[END_REF]. Four extraction controls were performed. Mammal and plant DNA was amplified with the primer pair P007, following the protocol described in [START_REF] Giguet-Covex | Long livestock farming history and human landscape shaping revealed by lake sediment DNA[END_REF]. In addition to extraction controls, we also performed three PCR controls, containing PCR mix but no DNA template. Four PCR positive controls were also performed, each of which contained 0.18 ng of DNA extracted from a marsupial (Didelphis marsupialis), that is not found in Europe. All samples and controls were amplified in 12 replicated PCRs [START_REF] Ficetola | Replication levels, false presences and the estimation of the presence/absence from eDNA metabarcoding data[END_REF]. Sequencing was performed by 2 × 125 bp pair-end sequencing on an Illumina HiSeq 2500 platform, which returned 21,192,000 reads.

DNA sequences were filtered using the OBITOOLS software [START_REF] Boyer | Obitools: a unix-inspired software package for DNA metabarcoding[END_REF], as described in [START_REF] Pansu | Reconstructing long-term human impacts on plant communities: an ecological approach based on lake sediment DNA[END_REF]. Sequences were assigned to the relevant taxa by comparing them with global databases of mammal and plant sequences that were generated from EMBL using the ecoTag program. For mammals, we only kept sequences with a match > 97% with a mammal genus. For plants, we focused on two species characteristic of the study area (pine: Pinus sp. and spruce: Picea sp.), and we only considered sequences with a match > 97% with the sequences of these species. The full set of sedDNA results will be published in a subsequent study (Chen et al. in prep.). In sedDNA studies, false detections (i.e., sporadic detections of absent species) are possible. We thus only considered species confirmed by multiple PCR analyses performed on the same sample, whereas we discarded sequences detected with < 5 reads in a given PCR replicate, and sequences frequently detected in the controls (human and pig).

Pollen and non-pollen palynomorphs (NPPs)

Following the same sampling that of sedDNA, 51 subsamples of approximately 1 cm 3 were prepared for pollens and non-pollens palynomorphs analysis, using the standard procedure described by [START_REF] Faegri | Textbook of Pollen Analysis[END_REF]. Lycopodium clavatum tablets were added to each subsample [START_REF] Stockmarr | Tablets with spores used in absolute pollen analysis[END_REF] in order to calculate the concentration of NPPs. They were counted following the procedure described by [START_REF] Etienne | Optimal counting limit for fungal spore abundance estimation using Sporormiella as a case study[END_REF] and are expressed as accumulation rates (no•cm -2 •yr -1 ). Their ecological interpretation in term of agro-pastoral activities and OM origin follows the work of [START_REF] Doyen | Ecological and human land-use indicator value of fungal spore morphotypes and assemblages[END_REF]. Non-arboreal pollen (NAP) was expressed as a percentage of the total pollen.

Chronology

The chronology of the Lake Verney sediment sequence is based on nine 14 C measurements performed on terrestrial plant macroremains, as well as short-lived radionuclide measurements ( 210 Pb and 137 Cs) to date the latest century. AMS radiocarbon dates were performed by accelerator mass spectrometer (AMS) at the Poznan Radiocarbon Laboratory and at the Laboratoire de Mesure 14C (LMC14) ARTEMIS at the CEA (Atomic Energy Commission) Institute of Saclay (Table 1). The 14 C ages were converted to 'calendar' years using the IntCal13 calibration curve [START_REF] Reimer | IntCal13 and Marine13 Radiocarbon Age Calibration Curves 0-50[END_REF]. Short-lived radionuclide were measured on the top of the sediment sequence at the Modane Underground Laboratory (LSM) by gamma spectrometry, using high-efficiency, very low-background, well-type Ge detectors [START_REF] Reyss | Large, low background well-type detectors for measurements of environmental radioactivity[END_REF]. The isotope 137 Cs was accidentally introduced into the environment at the end of the 1950s as by-product of atmospheric nuclear weapons tests (peak at AD 1963). The Chernobyl accident in 1986 also dispersed 137 Cs into the northern atmosphere [START_REF] Appleby | 241Am dating of lake sediments[END_REF]. 210 Pb excess ( 210 Pb ex ) results in the disintegration of 226 Ra of rocks into 222 Rn which disintegrates, in gas form, in 210 Pb ex in the atmosphere and deposited in the lake. It was calculated in the sediment as the difference between total 210 Pb (mixing of erosion and atmospheric deposits) and 226 Ra activity [START_REF] Goldberg | Geochronology with 210Pb[END_REF]. 226 Ra activity is assuming equivalent to 210 Pb activity of sediments triggered by erosion. Then, we used the Constant Flux/Constant Sedimentation (CFCS) model and the decrease in 210 Pb ex to calculate the sedimentation rates. The uncertainty of sedimentation rates obtained by this method was derived from the standard error of the linear regression of the CFCS model. The age-depth model was then generated using R software and the R code package 'Clam' version 2.2 [START_REF] Blaauw | Methods and code for "classical" age-modelling of radiocarbon sequences[END_REF].

2.4. Soil and sediment analysis 2.4.1. Loss on ignition Loss on ignition (LOI) analysis was performed on both the soil samples and sediments, following a continuous 1 cm sampling step all along the sediment sequence and every 3 cm using the sampling of DNA, pollens and NPPs analysis to estimate organic matter (OM) and carbonate content following the procedure described in [START_REF] Heiri | Loss on ignition as a method for estimating organic and carbonate content in sediments: reproducibility and comparability of results[END_REF]. OM content was measured on dried sediment after 4 h at 550 °C in an oven, then carbonate content was measured after 2 h at 950 °C.

P-XRF mineral geochemistry

A portable ED-XRF spectrometer (S1 TITAN Bruker) was used to measure the major elements, which were expressed as relative percentages of oxides. Analysis of both gently crushed soil and sediment samples was performed through a 4-μm-thick Ultralene film in a 32mm-diameter plastic cup. The samples were triplicated and analyzed over 60 s using the GeoChem Standard instrument's internal calibration mode [START_REF] Shand | Portable X-ray fluorescence analysis of mineral and organic soils and the influence of organic matter[END_REF]. The organic matter content that was deduced from the LOI at 550 °C was added to the sum of all major and trace elements. Consequently, the elemental results were brought to 100% less the OM percent to overcome the closed sum effects that are linked to OM variations [START_REF] Baize | Guide des analyses en pédologie: 2e édition, revue et augmentée[END_REF]. The standard deviations of the replicates were lower than the instrument errors, which were thus conserved as measurement uncertainties. The total contents of Fe and Al (Fe Tot and Al Tot ) were estimated from Fe 2 O 3 and Al 2 O 3 contents, respectively.

Extractable fractions

To identify pedogenetic compounds specific to Podzol spodic horizons in both the soil and sediment samples, we quantified the amount of secondary mineral phases containing Fe, Al and Si. Secondary Febearing phases were extracted from PSB1, PSB2, PSB3, PSB4 and PSB7 and secondary Fe-, Al-and Si-bearing were extracted from VERS1 and VERS2, and from 38 samples (each 1 cm thick) taken from the sediment core. For PSB1, PSB2, PSB3, PSB4 and PSB 7, the secondary Fe-bearing phase were extracted with three solutions of dithionite citrate, acid ammonium oxalate and 0.1 M Na pyrophosphate to quantify the crystalline, amorphous and organic-bound fractions in the samples, respectively [START_REF] Mckeague | Differentiation of forms of extractable iron and aluminum in soils[END_REF]. For VERS1 and VERS2 and the sediment samples, Al, Fe and Si were extracted only using an acid ammonium oxalate solution [START_REF] Tamm | Urn bestamning ow de organisk komponenterna i merkens gelkomplex[END_REF]. All of the extracts were then analyzed by ICP-AES. Soil pH was measured with a 1:5 soil-water ratio.

Statistical analysis

Principal component analysis (PCA) was performed on two sedimentary datasets that corresponded to the sampling strategy used for sedDNA, pollen and NPPs (3-cm-thick samples) and to the sampling strategy used for selective extraction (1-cm-thick-samplies), as well as on the soil geochemical parameters. PCA was used to assess the relationships between the elemental variations, human activities and soil dynamics in the catchment [START_REF] Sabatier | Clay minerals and geochemistry record from northwest Mediterranean coastal lagoon sequence: implications for paleostorm reconstruction[END_REF]. Analyses were performed using R 2.13.1 (R Development Core Team, 2011).

Results

Soil characterization

Apart from Cambisols, Leptosols, Regosols and sparse Podzols, the current soils of the Petit-Saint Bernard Pass area, at elevations between 1800 and 2700 m are mainly related to Stagnosols [START_REF] Moulin | Les séquences pédo-sédimentaires des versants du col du Petit Saint Bernard[END_REF].

Regosols, represented by VERS3, were identified in the south part of Lake Verney on black limestone (Fig. 1-c). They are thin, and only the coarse elements effervesce with HCl acid solution. pH is high (pH = 7.1). No horizons were distinguished in these soils but they received sediments from slope deposits. Thus, they may also develop on the upper slopes of the catchment, locally as Leptosols and Cambisols.

Stagnosols were found around the lake (VERS1, VERS2), within the pass (PSB7 but also Séez -Col du Petit Saint-Bernard -Sondage 14) and on the Italian side of the pass below the lake catchment near Plan Veyle at an elevation of 2000 m [START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF]. They are characterized by low pH (4.5) and low organic matter content in the mineral horizons (Fig. 2-a). Two types of mineral horizons, albic horizons in the subsurface and rust-colored horizons below, were noted in these soils (Fig. 2).

Podzols were found on the French side of the pass and are characterized by thick surface organic (O) horizon, with light gray (E) and rust (Bh and Bs) horizons below (Fig. 2-a, e.g., PSB3). Organic matter is also more important in the Bh horizons than in the eluvial E horizon. The pH values of these soils are also acid, in the same range of that of Stagnosols, between 3.7 and 4.8 (Fig. 2).

The amount of Fe extracted using ammonium oxalate acid and 0.1 Na-pyrophosphate solutions were < 2% in the Stagnosols and exceeded 2% in the spodic horizons of the Podzols, whereas the eluvial horizons showed very low (< 0.15%) amount of extracted Fe. Both Fe Ox /Fe Tot and Fe Pyr /Fe Tot ratios in Podzols follow the same trend: iron depletion in the eluvial horizons (ratios < 0.1) and enrichment in the spodic horizons (> 0.25). The Fe 2 O 3 /Al 2 O 3 ratio presents the same variations, but we note that there is more Al

2 O 3 than Fe 2 O 3 is present in the upper part of the spodic horizon (Fe 2 O 3 /Al 2 O 3 = 0.8) than in it lower part (Fe 2 O 3 /Al 2 O 3 = 1.2).
In contrast to the pattern displayed by Fe, the SiO 2 /TiO 2 ratio shows an increase in the eluvial horizon (SiO 2 / TiO 2 = 50) compared to spodic horizons (SiO 2 /TiO 2 = 25). In the Stagnosols, the ratios do not present such pronounced variation as those seen in the Podzols. The values of Fe Ox /Fe Tot and Fe Pyr /Fe Tot ratios are < 0.2, the values of Fe 2 O 3 /Al 2 O 3 are largely constant and range between 0.2 and 0.4, and the values of the SiO 2 /TiO 2 ratio are higher, ranging between 40 and 60.

Stagnosols are driven by hydrological processes and clogging of the surface (albic) horizons, especially during snowmelt, leading to the migration of Fe (II) and forming rust horizons below. Podzols are the result of the formation of organo-metallic compounds of Fe and Al in the surface horizons (O and E) and their migration with acidification from the eluvial horizon to the spodic Bh and Bs horizons.

Three paleosols were identified, in PSB1, PSB2 and PSB4 (Fig. 2-b). They correspond to old soils that are covered by deposits that are now developing new active soil layers. PSB1 and PSB2 display recurrences of albic and rust horizons (Fig. 2-b). The lowest rust horizons have high [START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF]. Four other levels occurring at depths of 15, 25, 52, and 58 cm within this profile were dated using Pinus charcoals to 2545, 2600, 4705 and 4725 cal. yrs BP. PSB4 presents an underlying succession of horizons similar to the PSB3 Podzols. Podzolic patterns were confirmed by the analysis of OM and extracted Fe. A Cambisol had developed on this paleopodzol.

Statistical analyses of the soil horizons

Fe Pyr , which represents the content of Fe-organic complexes, was not measured in the horizons of VERS1 and VERS2, but as Si Ox was < 0.01% in these horizons (data not shown), we considered that the abundances of amorphous compounds were negligible. Thus, we assumed that Fe Ox would be equal to Fe Pyr in VERS1 and VERS2 and carried out the PCA using a Fe Pyr /Fe 2 O 3 ratio for all the horizons.

The correlation circle from the PCA and its corresponding biplot map for the soil samples highlighted the relations between the different elements and ratios measured in soils horizons, and allowed us to characterize each type of horizon (Fig. 3-a). Dimensions 1 and 2 (denoted as Dim 1 and Dim 2) represent 72% of the total variability. Several end members were identified on the correlation circle. The first one, which is dominated by SiO 2 and the K 2 O/TiO 2 and Al 2 O 3 /TiO 2 ratios, is positively correlated with the first dimension of the PCA and opposite to Fe Pyr /Fe 2 O 3 that is poorly and negatively correlated with this first component. A second end members is positively correlated with the second component of the PCA and yields high positive loadings for TiO 2 , % Fe Ox , Fe 2 O 3 and Fe 2 O 3 /TiO 2 . It adjoins Fe Pyr and Fe 2 O 3 / Al 2 O 3 which are negatively correlated with Dim 1 and positively correlated with Dim 2. On the other hand, the SiO 2 /TiO 2 ratio is positively correlated with Dim 1 and negatively correlated with Dim 2. Moreover, the organic matter and CaO contents are negatively correlated with both components and anticorrelated with the K 2 O and Al 2 O 3 contents. Mapping of the horizons highlights the correlation between the surface O horizons and organic matter, and between the bleached (albic and E) horizons with SiO 2 /TiO 2 , but there is no possibility of distinguishing the eluvial horizons of the Podzols from the albic horizons of Stagnosols (Fig. 3-a). In contrast, this PCA allows us to distinguish spodic (Bs and Bh) horizons of the Podzols, which are highly correlated with % Fe Pyr and Fe 2 O 3 /Al 2 O 3 , from the rust horizons of the Stagnosols, which are positively correlated with both components of the PCA that are represented by Al 2 O 3 and K 2 O contents. The A and B horizons, which are poorly differentiated, are located in the middle of the map and are not associated with any component. The C horizons are characterized by poorly weathered material and are mainly related to the second component of the PCA, which is associated with the TiO 2 and Fe 2 O 3 contents. We note that the surface horizons are mainly negatively correlated with the second component, and the deeper horizons are positively correlated with this component. Apart from the E horizons, the first component permitted the separation of horizons experiencing podzolization which display positively correlated OM enrichment and spodic properties, from horizons with stagnic properties, where these characteristics are negatively correlated.

Lithology and sedimentological analyses

Based on macro-observations of the sediment surface and on the sedimentary and geochemical analyses presented in Fig. 4, four sedimentary units were identified.

Unit 4 (2.4 to 2.12 m) is composed of green-gray silts to sands and pebbles. The LOI at 550 °C presents the largest values of the sediment sequence. The grain-size distribution differs strongly from the rest of the sequence and is coarser with particles ranging in size from 40 to 200 μm (Fig. 4). The XRF-intensities of Ti and the contents of SiO 2 and Al 2 O 3 present the lowest values of the sequence. The Ca intensities and Fe 2 O 3 are variable whereas the SiO 2 /TiO 2 ratio remains constant.

Unit 3 (2.12 to 1.7 m depth) is made of dark gray silt and includes some orange layer that alternate with layers containing many macrofossils and sparse fine sandy layer (Fig. 4). Unit 3 includes the largest value of LOI at 950 °C and Ca intensities (approximately 25%). The grain size displays a slight fining-upward trend. All of the other geochemical parameters are highly variable, except for the SiO 2 /TiO 2 ratio that seems constant but is higher than in Unit 4.

Unit 2 (1.7 to 1.15 m depth) is composed of gray silt with alternating fine sand and orange patterns (Fig. 4). Both the Ca intensities and LOI at 550 °C decrease with time. The other parameters increase with time, except for the Al Ox /Al Tot and SiO 2 /TiO 2 ratio which remain constant; the latter ratio has higher values than the previous unit, and the Fe 2 O 3 /Al 2 O 3 ratio decreases in the upper part of the unit. The grain size does not show important variations.

Unit 1, which extends from a depth of 1.15 m to the top, is made of dark gray to brown silts and includes fine sand layer alternating with orange patterns (Fig. 4). The 550 °C LOI is quite constant in this unit, approximately 5%, and the LOI 950 °C varies slightly at the bottom of the unit and is slightly larger with an average value of 12%, than in the upper part of the unit (< 10%). The NCIR increases slightly from the bottom of the unit (85%) to the top (92%). The grain size distribution in unit 1 seem to be quite homogeneous, although a higher concentration of particles with sizes of approximately 20 μm occur in the upper part of the unit. The Ti intensities are higher and vary more than in the other units. The Si Ox values are very low and increase slightly in parallel with SiO 2 content. Both Al Ox and the Al Ox /Al Tot ratio are higher in the bottom part of the unit and decrease from the bottom to the top. Fe Ox and the Fe Ox /Fe Tot ratio increase from the bottom part of Unit 1 to a depth of 0.7 m and then decrease to the top. The Fe 2 O 3 /Al 2 O 3 ratio displays important variations in the bottom part of unit 1 and is more nearly constant in the upper part. The SiO 2 /TiO 2 ratio varies rapidly and increases in the upper 0.15 m.

Age-depth model

A total of 9 radiocarbon analyses were performed on selected macrofossils collected from the 2.4-m length of the sediment core (Table 1). Three radiocarbon dates were excluded from the age-depth model (bold in Table 1). Samples Poz-73372 and Poz-73373, which were dated to 8000 and 4615 BP, respectively, are clearly as too old: their macrofossils had probably been reworked, and the corresponding ages have been removed from the age-depth modeling. The third excluded sample (Poz-73374) was associated with a change in the sedimentation rate that also corresponds to the change of sedimentary units (units 2 and 1). Thus, for the age-depth model constructed using the Clam routine, this date was excluded to better reflect the change between these sedimentary units (Fig. 5-a). The model was computed with a smooth relation until SacA-32339 and interpolated below.

The measurement of short-lived radionuclides allowed the dating of the uppermost 7 cm of the core [START_REF] Appleby | The calculation of lead-210 dates assuming a constant rate of supply of unsupported 210 Pb to the sediment[END_REF]. A logarithmic plot of 210 Pb ex activity (Fig. 5-b) shows a downward decrease from the surface. According to the 'constant flux, constant sedimentation rate' (CFCS) model [START_REF] Goldberg | Geochronology with 210Pb[END_REF][START_REF] Krishnaswamy | Geochronology of lake sediments[END_REF], the levels of 210 Pb ex indicate a mean accumulation rate of 0.7 mm•yr -1 . The 137 Cs activity profile (Fig. 5-b) has a peak at a depth of 4.05 ± 0.25 cm and reaches a maximum at 2.05 ± 0.25 cm, interpreted respectively as the beginning of atmospheric production of 137 Cs, in 1955 (due to nuclear tests) and the Chernobyl accident in 1986 [START_REF] Robbins | Determination of recent sedimentation rates in Lake Michigan using Pb-210 and Cs-137[END_REF]. The expected high 137 Cs activity associated with the maximum intensity of nuclear weapons testing in the Northern Hemisphere in AD 1963 may lie between these two depths; however, it is not clearly identifiable likely due to both the low resolution of the analyses and the large amount of fallout from Chernobyl. The good agreement between the ages of the artificial radionuclide peaks inferred from the 210Pbex-CFCS model (1956 and 1984) and the actual ages of artificial radionuclide peaks (1955 and 1986) suggests that these dates provide an accurate and continuous age-depth relationship within the upper 7 cm of the sediment sequence. These data M. Bajard et al. Geoderma 306 (2017) 217-236 were incorporated into Clam to generate the age-depth model of the whole core alongside the 14 C age estimates (Fig. 5-a).

% Fe Ox % Fe Pyr % OM Al 2 O 3 SiO 2 K 2 O TiO 2 Fe 2 O 3 Al 2 O 3 /TiO 2 K 2 O/TiO 2 Fe 2 O 3 /TiO 2 SiO 2 /TiO 2 Fe OxPyr /Fe 2 O 3 O Albic Rust C E Al 2 O 3 SiO 2 K 2 O TiO 2 % OM SiO 2 /TiO 2 Al Ox /Al 2 O 3
The age-depth model shows three major phases with differing sedimentation rates within the 2.4 m of the sediment sequence (Fig. 5-a). Units 4 and 3 span the period from 11,200 to 9200 cal. yrs BP and have a mean sedimentation rate of 0.7 mm•yr -1 (Fig. 6-a). Unit 2 covers the period between 9200 and 2400 cal. yrs BP and has a mean sedimentation rate of 0.07 mm•yr -1 . The sedimentation rate of unit 1 increases from 0.2 to 0.7 mm•yr -1 over the last 2400 cal. yrs BP up to the present (Fig. 6-a).

The variations in the values of the Pb/Ti ratio measured using the XRF core scanner show four periods of increases in Pb intensity (Fig. 5a). At the bottom of the core, before 10,000 cal. yrs BP, Pb is considered to be linked to the organic matter within the sediment. After 10,000 cal. yrs BP, the three other increases are consistent with the Roman period, the Medieval period and modern emissions of leaded gasoline, respectively, and these peaks support our age-depth model [START_REF] Arnaud | A 300 year history of lead contamination in northern French Alps reconstructed from distant lake sediment records[END_REF][START_REF] Elbaz-Poulichet | A 3500-year record of hg and Pb contamination in a Mediterranean sedimentary archive (the Pierre Blanche Lagoon, France)[END_REF].

Quantification of non-arboreal pollen (NAP) and NPPs

On average, NAP represents 16% of the total pollen from 11,400 to 3000 cal. yrs BP (Fig. 6-h). It increases from 3000 to 2000 cal. yrs BP to a maximum of 42%. NAP is once again at an average of 16% from 2000 to 1100 cal. yrs BP and increases again (up to 50%) after 1100 cal. yrs BP.

Among NPPs, we focus only on fungal ascospores produced in the catchment that grow on plant remains, within the soil litter, and in fecal material. Cercophora sp. (HdV-112), Coniochaeta ligniaria (HdV-172) and Kretzschmaria deusta (HdV-44) are assumed to be saprophytic fungal ascospores associated with the degradation of the litter associated with deciduous trees [START_REF] Doyen | Ecological and human land-use indicator value of fungal spore morphotypes and assemblages[END_REF]), whereas Sordaria sp. (HdV-55B), Sporormiella sp. (HdV-113) and Podospora sp. (HdV-368) are saprophytic/coprophilous or strictly coprophilous fungal ascospores [START_REF] Etienne | Optimal counting limit for fungal spore abundance estimation using Sporormiella as a case study[END_REF][START_REF] Doyen | Ecological and human land-use indicator value of fungal spore morphotypes and assemblages[END_REF][START_REF] Etienne | Influence of sample location and livestock numbers on Sporormiella concentrations and accumulation rates in surface sediments of Lake Allos, French Alps[END_REF]. NPP types were summed relative to their saprophytic or fecal ecological indicator value and expressed in abundances (no•cm -3 ) and accumulation rates (no•cm -2 •yr -1 ) (Fig. 6-f-g).

The abundances of saprophytic spores increase from 11,400 cal. yrs BP to a maximum at approximately 9000 cal. yrs BP. They decrease progressively until 3200 cal. yrs BP. On the other hand, accumulation rates remain low during the early and mid-Holocene, except between 3500 and 3900 cal. yrs BP (Fig. 6-f). The accumulation rates of saprophytic NPPs and their abundances follow the same trend during the last 3000 years, with four major increases occurring from 2600 to 2000 cal. yrs BP, 1600 to 1300 cal. yrs BP, 900 to 700 cal. yrs BP and Geoderma 306 ( 2017) 217-236 500 to 300 cal. yrs BP.

The abundances and accumulation rates of coprophilous ascospores both remain low until 4400 cal. yrs BP (< 10 spores and < 20 spore•cm -2 •yr -1 , respectively (Fig. 6-g)). The abundances of these spores reach 20 spores between 4400 and 4000 cal. yrs BP and a maximum value between 3000 and 2000 cal. yrs BP (45 spores). They remain high during the last 2000 years (10 to 35 spores), with small decreases occurring between 1800 and 1200 cal. yrs BP and 300 and 100 cal. BP. The accumulation rates increase progressively from 4000 to 800 cal. yrs BP, up to 250 spore•cm -2 •yr -1 , and remain high (100 to 200 spore•cm -2 •yr -1 ), with short-term decreases occurring at approximately 700 cal. yrs BP and during the last 150 years (Fig. 6-g).

Sedimentary DNA

The DNA of five mammalian taxa was found in the sediments of Lake Verney, specifically Bos sp. (cattle), Equus sp. (horse), Felis sp. (cat), Ovis sp. (sheep) and Sus sp. (pig). Equus, Felis and Sus were only detected in one or two samples within the sequence. Because these animals are uncommon in alpine pasture contexts, we focus only on DNA of Bos sp. and Ovis sp. (Fig. 6-j). No DNA from either Ovis or Bos was detected in sediments older than 2360 cal. yrs BP. DNA of Ovis sp. was found in 10 samples from 2360 to 200 cal. yrs BP. In samples with ages ranging from 2360 to 900 cal. yrs BP, sheep DNA was generally detected in multiple replicate PCR analyses per sample, whereas it was only detected in one out of 12 PCR replicates after 900 cal. yrs BP. DNA of Bos sp. was only detected in one PCR replicate between 2360 and 900 cal. yrs BP. After 900 cal. yrs BP, Bos DNA was found in 8 samples, in 1 to 3 positive PCR replicates per samples.

There are currently no trees in the catchment of Lake Verney. Among the DNA of trees found in the sediments, Pinus is a pioneer species in the Alps whereas Picea became established in the region at ca. 3000 yrs BP [START_REF] David | Évolutions de la limite supérieure des arbres dans les Alpes françaises du Nord depuis la fin des temps glaciaires[END_REF][START_REF] De Beaulieu | Dynamique forestière holocène dans la haute vallée de l'Arve (Haute-Savoie) et migrations de Abies et Picea dans les Alpes occidentales[END_REF]. Pinus DNA was found in at least one replicate in all samples with ages between 11,200 and 2900 cal. yrs BP, with an average of 5 positive replicates per sample (Fig. 6-i). During the second part of the Holocene, the number of positive replicates decreased. It was then found in between 0 and 2 replicates since 2900 cal. yrs BP, except between 1000 and 900 cal. yrs BP and in the most recent sample (4 positive replicates). Picea DNA appears punctually at ca. 6000, 5000 and 4000 cal. yrs BP with just one positive replicate (Fig. 6-i). After 3000 cal. yrs BP, it was detected more often, with up to 4 positive replicates per sample, especially between 2600 and 1000 cal. yrs BP.

Statistical endmembers

In order to avoid the influence of the bottom of the sediment sequence, which shows substantial variations in composition and sedimentation rates, PCA analyses were only performed on sediments with ages of 7000 years or less.

The first two components of the PCA performed using the data set of sediment selective extractions (n = 32) represent 71% of the variability (Fig. 3-b). The arrangement of variables according to both dimensions is similar to the PCA results from the soil samples. However, OM is more closely related to variations in iron, and it is positively correlated with the first component and negatively correlated with the second one, and the Fe 2 O 3 and TiO 2 contents appear to be drawn toward the axis of the first component and its terrigenous endmembers. The sedimentation rate (SR) and NCIR are also related to this group, supported by the first component. SiO 2 /TiO 2 is always positively correlated with the first component and negatively with the second one, while the calcium carbonate content is negatively correlated with both components. Finally, the values of the Al Ox /Al Tot ratio in the sediment seem to follow the same changes in the iron ratios and the OM contents.

The first two dimensions of the PCA performed using the data set including NAP, Pinus DNA and spore abundances of Kretzschmaria deusta, Cercophora-type, Coniochaeta ligniaria, Sordaria sp. and Sporormiella sp. represent 56% of the total variability (Fig. 3-c), and the resultst of this PCA appear to reproduce the same scheme as the PCA of the data set including selective extraction of Fe and Al (Fig. 3-b). Four endmembers can be identified. NAP, which is positively correlated with the first component, is strongly linked to the elements of terrigenous origin and ratios involving those elements. In contrast, CaO content, Pinus DNA, the spores of Kretzschmaria deusta, Fe 2 O 3 and Al 2 O 3 form a second group and are negatively correlated with the first group. A third endmembers that is associated with OM content and Sordaria and Coniochaeta ligniaria spores show a weak positive correlation with the second component of the PCA. Spores of the Cercophora-type are located between these two last endmembers and are positively correlated with the first component and negatively with the second one. As Ovis and Bos DNA occur sporadically in the sediment, their representativeness is poor in the PCA. Ovis DNA seems to be associated with both OM and terrigenous inputs. On the other hand, Bos DNA is especially closely related to the terrigenous endmembers and the sedimentation rate and by the SiO 2 /TiO 2 ratio. These components make up the fourth endmember, which is positively correlated with the first component and negatively correlated with the second one. The spores of Sporormiella sp. are situated between the directions of Ovis and Bos DNA, which is consistent with their relationship to pastoralism [START_REF] Etienne | Optimal counting limit for fungal spore abundance estimation using Sporormiella as a case study[END_REF][START_REF] Doyen | Ecological and human land-use indicator value of fungal spore morphotypes and assemblages[END_REF].

The biplot mapping of the results of both sediment PCAs according to the ages of the sediment samples shows a gradation along the first component, from the oldest sediments (7000-3000 cal. yrs BP), which are negatively correlated with the first axis, to the more recent sediment (1000 cal. yrs BP to the present), which are positively correlated with the first axis (Fig. 3-b-c). The sediments of the period between 3000 and 1000 cal. yrs BP are situated in the middle of the first axis and seem to be more closely associated with the second component.

Discussion

Sediment origins

Sediment inputs in the lake represent both changes in the pedolandscape around Lake Verney and the diversity of that pedo-landscape, just as the current soils do, and areas of preferential erosion. These sediments continuously record a mix of different sources, depths and degrees of weathering, including, in a global way, the expected dominant processes. They also record the main eroded areas that are the steepest slopes, mainly upstream, surrounding the lake and areas where erosion is induced by human activities. The steep slopes concern only Regosols or Leptosols that are expected to provide always the same constant contribution through time, downstream and to the sediment record. The study of erosion before the development of human activities, i.e., on long time-scale, allows us to dissociate this erosion source from the expected human induced erosion, assuming that other more advanced soil types are few eroded in the absence of human activity. Our goal is to differentiate the main sources of material, referring to the main pedogenetic processes that have occurred in the catchment. Both carbonate schist in the west and black shales in the east can provide Fig. 6. Evolution of pedo-landscapes and agro-pastoral activities in the Lake Verney catchment during the Holocene as inferred from a) sedimentation rates (SRs) and terrigenous fluxes (including 950 °C LOI and NCIR of the sediment); b) SiO 2 /TiO 2 ; c) Fe Tot /Al Tot ; d) Al Ox /Al Tot and e) Fe Ox /Fe Tot ratios to characterized the different sources of the soil horizons. The sum of saprophytic NPPs, including Coniochaeta ligniaria, Cercophora sp. and Kretzschmaria spores refers to the origin of the OM (f). Dung residue spores (g) represents the sum of Sordaria sp., Sporormiella sp. and Podospora sp. NAP is the sum of non-arboreal pollens (h). Tree DNA includes Pinus sp. and Picea sp. positive replicates (i), and mammal DNA (j) includes cow or sheep DNA positive replicates.

M. Bajard et al. Geoderma 306 (2017) 217-236 calcium (through dissolution) and calcium carbonates (through physical erosion) in the lake. Calcium carbonates recorded in the sediment may come from both terrigenous and authigenic inputs, but both inputs can reflect early conditions of soil development (decarbonatation), with small inputs of weathered material or the loss of carbonate material from young soils at the beginning of pedogenesis and associated with the rejuvenation of soils, e.g. on steep slopes [START_REF] Bajard | Progressive and regressive soil evolution phases in the Anthropocene[END_REF]. The OM contents recorded in the sediments are constant over the last 10,000 yrs, whereas the sediment flux has increased. This result suggests that the OM was derived from the catchment and was not produced authigenically in the lake. The terrestrial origin of the OM is supported by the record of saprophytic fungi spores, which show comparable abundances before and after the increase in erosion (Fig. 6f).

Record of soil footprints in the sediments

Identification of the soils that fed the lake sediments is made possible by the characterization of current soils on both hillsides of the pass and by the high differentiation of horizons between the soil types identified and within the same soil. Both the soils of the lake catchment and the soils close to the lake catchment were compared to the sediment record in order to catch all pedogenetic processes that could no longer operate in the lake catchment. Soils and especially paleosols were also considered to validate our interpretation from the sediment sequence. The development of undifferentiated and thin Regosols on limestone, whereas the other soils are acid, suggests that the decarbonatation from rock to soil during weathering is relatively fast. Only the coarse fragments in the matrix effervesce to HCl solution, and these elements can provide terrigenous carbonates to the lake. This quick acidification also allowed the development of Podzols on material that had previously been leached of carbonate (e.g., PSB3 and PSB4) over relative short timescales (e.g., [START_REF] Bormann | Rapid soil development after windthrow disturbance in pristine forests[END_REF].

Both Podzols and Stagnosols are very acid soils (pH 4 to 5, e.g., PSB3 and VERS2); thus, they can develop from acid Cambisols. Both are characterized by different horizons, albic and rust in particular.

Identified albic horizons

The albic horizons of both the Podzols and Stagnosols are characterized by a light color ("bleached" or "whitened") and are enriched in silica (high ratios of SiO 2 /TiO 2 ), reflecting the eluvial character of these horizons (Figs. 3-a and7). In consequence, they are difficult to distinguish, except for the E horizons of Podzols. These horizons occur between OM-rich horizons; thus, they are more often associated with organic matter than albic horizons, which are conversely more closely associated with strictly terrigenous materials, such as SiO 2 , K 2 O and Al 2 O 3 (Figs. 3-a and7).

Differentiation of the rust horizons of Stagnosols from the spodic horizons of Podzols

The rust horizons of Stagnosols and the spodic horizons of Podzols are well differentiated by different variables with regard to the PCA performed on the soil samples (Fig. 3-a). The spodic horizons are characterized by high values of Fe Ox , Fe Pyr , and Fe Tot /Al Tot , whereas the rust horizons of Stagnosols are more strongly characterized by K 2 O and Al 2 O 3 . Organo-metallic complexes of Al and Fe form in the sub-surface horizons of Podzols and accumulate in the Bh and Bs horizons (Fig. 7). Al-OM complexes can accumulate to a greater degree in Bh horizons under hydromorphic conditions [START_REF] Anderson | A reassessment of podzol formation processes[END_REF][START_REF] Legros | Les grands sols du monde[END_REF]. Based on the studies of [START_REF] Mourier | Distinguishing subalpine soil types using extractible Al and Fe fractions and REE geochemistry[END_REF][START_REF] Mourier | Soil evolution and subalpine ecosystem changes in the French Alps inferred from geochemical analysis of lacustrine sediments[END_REF], these geochemical proxies are the characteristics that we will look for in the sediment, assuming their conservative behavior during mobilization, transport and deposition from the catchment to the lake and that they did not form in the lake (Fig. 7). This assumption is possible considering the small size of the lake catchment, and the smaller areas in the catchment concerned by soils and not only scree. Climatic and pH conditions are also in favor of low biological and chemical changes of soil-sediment properties within the lake (i.e., low temperatures and higher pH in soils than in the lake).

Only extractions with ammonium oxalate solution were performed on sediment samples. Fe Ox , Al Ox , and Si Ox represent the amount of both amorphous and complexed forms, whereas extractions with Na-pyrophosphate only extract the complexed forms. The Podzols are characterized by the presence of OM-complexes and the small differences between Fe Pyr and Fe Ox seen in PSB3 and PSB4. These results indicate that little or no amorphous material was present in the Podzols. The very low contents of Si Ox in the sediment indicate that there are no amorphous compounds of Si, and thus we assumed that there are also no amorphous compounds of Fe and Al, as we did for the horizons of VERS1 and VERS2. Furthermore, the microbial activity of the lake could change Fe-OM complexes into amorphous compounds [START_REF] Birkeland | Soils and Geomorphology[END_REF][START_REF] Mourier | Soil evolution and subalpine ecosystem changes in the French Alps inferred from geochemical analysis of lacustrine sediments[END_REF]. In consequence, the contents of Fe Ox and Al Ox are attributed to the OM-complexes of spodic horizons. Finally, as the sediment reflects a mixture of different sources, we normalized Fe Ox and Al Ox to the contents of total iron (% Fe 2 O 3 ) and aluminum (% Al 2 O 3 ), respectively, to trace the inputs from spodic horizons into the lake (Fig. 7). In the PCA performed using data from the selective extractions of sediments (Fig. 3-b), both the Fe Ox /Fe Tot and Al Ox /Al Tot ratios are strongly correlated with the Fe Tot /Al Tot that strongly characterizes the spodic horizons, thus supporting our interpretation.

4.3. Evolution of soils and agro-pastoral activities throughout the Holocene, as inferred and dated from sediment archives of Lake Verney 4.3.1. 11,000 to 4300 cal. BP: from decarbonatation of the catchment to acidification of soils

The composition and chronology of unit 4, which was deposited between 11,200 and 11,100 ± 100 cal. yrs BP suggests instantaneous deposition of this unit, similar in its carbonated nature to the parent material, at the beginning of the lake sedimentation (Figs. 1, 4 and5-a). The sedimentation dated to 11,100 and 10,000 cal. yrs BP is rapid but lower than the sedimentation rates seen in unit 4 and displays a high variability in the OM contents and the values of the Fe 2 O 3 /Al 2 O 3 ratio.

Between 10,000 and 4300 cal. yrs BP, erosion was lower, and Pinus DNA became abundant (Fig. 6-i). The high abundance of charcoals of Pinus cembra found in four soil profiles in the area of the pass confirms that the DNA recorded in Lake Verney come from this species [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF]. Five of them were found at 1940 m on the French side of the pass and were dated to between 4325 and 3910 cal. yrs BP [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF], in agreement with the chronology of Pinus DNA in the sediment (Fig. 6-i). The abundance of saprophytic spores between 10,000 and 4300 cal. yrs BP, confirms the development of litter horizons under the forest (Fig. 6-f). At the same time, the carbonate contents decrease and the values of Fe Ox /Fe Tot ratio increase, suggesting that organic acids from the forest litter contributed to the dissolution of the soil carbonates and acidified the soils, permitting dissolution of Fe, which formed complexes with OM compounds and migrated through the soils, and could be laterally transported into the lake. The change in carbonate contents in the early to mid-Holocene sediment appear to have been controlled mainly by weathering of the catchment, favored by forest covers [START_REF] Giguet-Covex | Changes in erosion patterns during the Holocene in a currently treeless subalpine catchment inferred from lake sediment geochemistry (Lake Anterne, 2063 m a.s.l., NW French Alps): the role of climate and human activities[END_REF][START_REF] Dreibrodt | Lake Belau and its catchment (northern Germany): a key archive of environmental history in northern central Europe since the onset of agriculture[END_REF][START_REF] Bajard | Progressive and regressive soil evolution phases in the Anthropocene[END_REF]. The values of Al Ox /Al Tot ratio do not vary within the sediment deposited during this period, perhaps due to the lower mobility and lower contents of Al Ox compared to Fe Ox . In consequence, it is possible that the Al complexes migrated within the soils, as did the Fe complexes, forming spodic horizons but not reaching the lake. The development of spodic horizons is corroborated by the increase in the values of the Fe Tot /Al Tot ratio in the lake sediment between 10,000 and 4300 cal. yrs BP. Moreover, the time between the beginning of pedogenesis and 4300 cal. yrs BP seems long enough to allow the differentiation of such horizons [START_REF] Bormann | Rapid soil development after windthrow disturbance in pristine forests[END_REF][START_REF] Protz | Rate of podzolic soil formation near Hudson Bay, Ontario[END_REF]. Pedogenesis may have been favored by the climate warming that occurred during this period, which is assumed to have reach its maximum between 6000 and 7000 cal. BP [START_REF] Millet | Les assemblages de chironomidae et les cortèges polliniques, outils de reconstitutions quantitatives des changements du climat Holocène: une approche croisée au col du Petit Saint Bernard[END_REF]. Thus, following the loss of carbonate compounds, acidification led to the development of Podzols in the catchment of Lake Verney, where no Podzols are currently present. Neither DNA nor NPPs indicate human activities in the Lake Verney catchment before 4300 cal. yrs BP.

4300 to 2600 cal. BP: first human occupation in the catchment: deforestation and litter erosion

From 4300 cal. yrs BP, erosion increased gradually from 0.004 to 0.008 g•cm -2 •yr -1 and forest reduction and inputs of coprophilous fungi spores represent the first opening of the landscape to human activities in the catchment (Fig. 6-a-h-i). Fire episodes inferred from the anthracological study of [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF] are consistent with forest clearing at this altitude and during this period. The migration of Picea into the area of the pass may have been favored by human activities [START_REF] Miras | Dynamique des écosystèmes et impact de l'homme dans le secteur du col du Petit Saint Bernard au cours de l'Holocène[END_REF].

The variability in Kretzschmaria deusta and Coniochaeta ligniaria was related to the Pinus DNA and the OM contents, respectively (Fig. 3-c) and suggest an erosion of litter and soil organic horizons between 4000 and 3600 cal. yrs BP (Fig. 6-f). Erosion of surface soil horizons could explain the substantial amount of Pinus DNA detected when clearing was initiated. On the other hand, the absence of mammal DNA in the sediment could reflect a low intensity of pastoral activities.

After 3800 cal. yrs BP, the input of albic material increased (Fig. 6b). Following the erosion of the organic horizons, erosion of the eluvial horizons of the Podzols seems to be the most convincing hypothesis for this increase, but we cannot exclude erosion of the albic horizons of the Stagnosols. Indeed, the albic and rust horizons of the Stagnosols are more closely associated with TiO 2 , Al 2 O 3 and SiO 2 than the E horizons of the Podzols (Fig. 3-a), suggesting that the first record of stagnic horizons occurred between 2900 and 2600 cal. yrs BP (Figs. 4 and6).

2600 to 1000 cal. BP: erosion of spodic horizons

During the Second Iron Age and the Roman period, pastoral activity steadily increased, as reflected by the occurrence of substantial amounts of NAP, whereas the detection of tree DNA diminishes (Fig. 6g-h-i). According to the mammal DNA, more sheep flocks than herds of cows were going up to pasture around the pass during this period (Fig. 6-j). In association with this intensification of pastoral activities, the erosion rate strongly increased between 2600 and 1900 cal. yrs BP, as both of the Al Ox /Al Tot and Fe Tot /Al Tot ratios, followed by the increase in Fe Ox /Fe Tot after 1900 cal. yrs BP, indicating the successive erosion of the Bh and Bs spodic horizons of the Podzols (Fig. 6-a-c-d-e). This result indicates that the erosion of the albic horizons during the previous period was more closely associated with eluvial horizons than the albic horizons of Stagnosols. The variability in the values of SiO 2 /TiO 2 and Fe Ox /Fe Tot ratios between 1900 and 1000 cal. yrs BP seems to indicate mixing with material from albic horizons, especially between 1600 and 1400 cal. yrs BP when lower values of the Fe Tot /Al Tot ratio are noted. Except for SiO 2 /TiO 2 , the values of all the ratios (i.e., Al Ox /Al Tot , Fe Ox / Fe Tot and Fe Tot /Al Tot ) began to decline around 1900 cal. yrs BP, suggesting a change in pedogenetic processes, from podzolization to the development of stagnic properties. Erosion of the Bh and Bs horizons is supported by the occurrence of the two periods during which the largest terrigenous fluxes took place and by the terrestrial OM inputs (Fig. 6-af), which could reflect the organic character of the eroded horizons, and could have been transported with the Al and Fe-OM complexes [START_REF] Wilmshurst | Origin of pollen and spores in surface lake sediments: comparison of modern palynomorph assemblages in moss cushions, surface soils and surface lake sediments[END_REF].

Between the Antiquity and the Middle Ages, during the so-called "Dark Ages", a significant decrease in the NAP associated with an increase in the tree DNA was recorded, indicating recolonization of the site by pine (likely Pinus cembra) and spruce (Fig. 6-h-i). In a few short centuries, this recolonization could have led to a recovery in podzolic processes as suggested by the slight increases in the spodic ratios (i.e., A lOx /Al Tot , Fe Ox /Fe Tot and Fe Tot /Al Tot ). This recovery of the forest is supported by both human and climate forcing. Hearths found around the Roman building were dated to between 1834 and 1580 cal. yrs BP [START_REF] Rey | Le Cercle de pierres dressés du Col du Petit Saint-Bernard (Savoie -Val d'Aoste, 2188 m d'altitude) Nouvelles données de terrain et pistes d'interprétation[END_REF]. These dates are in accordance with the old coin inventory of [START_REF] Rémy | Les monnaies Antiques découvertes au col du Petit SAint Bernard (versants Français et Italien)[END_REF], and suggest at least use of the pass at that [START_REF] Anderson | A reassessment of podzol formation processes[END_REF]. **In our case, the very low content of Si Ox in the sediments (Figure 4) justified the absence of amorphous compounds allowing to consider only oxalate solution to extract organo-metallic complexes. (Furthermore, organo-metallic complexes could be transformed in amorphous material due to mineralization during erosion and transfer to lake sediment). time. The destruction of the Roman building at approximately 1600 cal. yrs BP and the occurrence of a colder period recorded approximately 1700 cal. yrs BP [START_REF] Millet | Les assemblages de chironomidae et les cortèges polliniques, outils de reconstitutions quantitatives des changements du climat Holocène: une approche croisée au col du Petit Saint Bernard[END_REF] could be related to abandonment of the area and the beginning of this new, short-live pedogenetic phase.

1000 cal. BP to present: development of stagnic properties

From 1000 to 100 cal. yrs BP, erosion rates continued to increase, from 0.04 to 0.06 g•cm -2 •yr -1 . Between 1000 and 400 cal. yrs BP, mammal DNA, NAP and the spores of coprophilous fungi spores reach their maxima (Fig. 6-h-i-j). They increase again between 400 cal. yrs BP and the present. During both of these periods, the occurrence of tree DNA remains sporadic, indicating that clearing was maximum, as it does today, without trees in the catchment. The most important change in pastoral activities is reflected by the most pronounced detection of Bos DNA that suggests an increase in cattle breeding after the Middle-Ages. Indications of podzolization become more and more sparse, and the development of stagnic properties has dominated pedogenesis since at least 400 cal. yrs BP.

Validation of soil evolution with current soils, paleosol and anthracological analyses

The current soils, the studied paleosols, plus the anthrocological study performed by [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF], in the area of the Petit Saint-Bernard Pass as part of the Alpis Graia Interreg Project, provide elements that support the soil evolution scenario proposed using the sediment record from Lake Verney.

First, the current pedogenesis of the lake catchment, dominated by stagnic properties, is consistent with the interpretation of the latest sediment deposits. No evidence of Podzols was found in the lake sediment for the last 400 years cal. BP, in agreement with the current absence of Podzols in the catchment of Lake Verney. Podzols can develop at higher altitudes than those found on the French side of the pass (e.g., PSB3) and on the black shales of the Houillere Briançonnais area and below the subalpine Rhododendron heaths, as reported by [START_REF] Mourier | Distinguishing subalpine soil types using extractible Al and Fe fractions and REE geochemistry[END_REF]. The development of true Podzols is also possible on calcareous schists (obviously after decarbonatation), and in wet climates, such as those found in the Northern Alps [START_REF] Legros | Soils of Alpine mountains[END_REF]. Podzols developed on Liassic calcareous schists have been described from the Balme Pass (2200 m), located 40 km to the north of the Petit Saint-Bernard Pass [START_REF] Dambrine | Contribution à l'étude de la répartition et du fonctionnement des sols de haute montagne: massifs des Aiguilles Rouges et du Mont-Blanc[END_REF]. Thus, the current absence of Podzols around Lake Verney cannot result from the altitude of the lake, which is above 2088 m, nor from the geological materials underlying the catchment.

Clear evidence of spodic horizons were identified in the sediment record, especially between the mid-Holocene period and the Middle Ages. Paleopodzols like those seen in PSB4 have been found at lower altitudes (2000 m) on the French side of the pass, indicating that old, but undated Podzols had developed and were subsequently covered by erosion induced deposits. Erosion increased beginning 4300 cal. yrs BP; thus, it is possible that Podzols were present before 4300 cal. yrs BP. Moreover, the deepest charcoals found within a Podzol (beyond the organic-mineral horizon) at 1940 m of elevation were dated to 1210 and 4160 cal. yrs BP [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF]. The other 8 dates obtained from this profile ranged from 2105 to 4325 cal. yrs BP, except for one sample that yielded an age of 330 cal. yrs BP and was obtained from the organic surface horizons. These charcoals indicate that fire episodes occurred during this interval, and that Podzols were present in the area of the pass before the Roman period and before the strong increase in erosion.

Among the successive albic and rust horizons of both paleosols PSB1 and PSB2, the deepest rust horizons display high contents of Fe Ox , and slightly more Fe Pyr was noted in PSB1 (at depth of approximately 30 and 40 cm). These characteristics are reminiscent of the spodic character of the Podzols, even if the values are 2 to 3 times less important than for Podzols (Fig. 2). The other albic and rust patterns do not display these characteristics. Our hypothesis is that these deep, Fe Ox -enriched horizons represent old degraded spodic horizons. Removal of the surface horizons and their exposure could allow the mineralization and degradation of organo-metallic complexes and the formation of amorphous compounds, e.g., ferrihydrite, suggested by the high ammonium oxalate extractable Fe fraction [START_REF] Birkeland | Soils and Geomorphology[END_REF][START_REF] Stucki | Soil sampling and isolation of extracellular DNA from large amount of starting material suitable for metabarcoding studies[END_REF]. OM-complexed forms can oxidize due to drainage and form ferrihydrite. This process is characteristic of acid hydromorphic soils [START_REF] Jeanroy | Diagnostic des formes du fer dans les pédogénèses tempérées: évaluation par les réactifs chimiques d'extraction et apports de la spectrométrie Mossbauer[END_REF]. Hydromorphic processes may have been present in the Podzols but had only a weak effect while podzolization occurred.

Furthermore, if we consider the thicknesses of the Podzols currently found in the area of the Petit Saint-Bernard Pass, to the Bs horizons, i.e., approximately 30 cm (PSB3, Fig. 2-a), and the period during which the Podzols were eroded, approximately 3000 yrs (between 4000 and 1000 cal. BP), the potential erosion rate is 0.1 mm•yr -1 on average. This order of magnitude falls within the range of erosion rates triggered by agricultural management over the last two millennia [START_REF] Enters | Historical soil erosion and land-use change during the last two millennia recorded in lake sediments of Frickenhauser See, northern Bavaria, central Germany[END_REF][START_REF] Massa | A 2500 year record of natural and anthropogenic soil erosion in South Greenland[END_REF][START_REF] Bajard | Progressive and regressive soil evolution phases in the Anthropocene[END_REF]. It is also in the commonly admitted range of soil formation rates [START_REF] Montgomery | Soil erosion and agricultural sustainability[END_REF][START_REF] Larsen | Rapid soil production and weathering in the southern Alps[END_REF] and raises the question of the sustainability of the pasture, which appears to be in equilibrium with the activities taking place in the catchment.

Charcoals were only found in PSB1 and were dated. Six 14 C dates provide information on the different levels and hearths found within the soil (Fig. 2). The deepest horizons were dated to 4725 and 4705 cal. yrs BP. Just below, the deepest hearth was dated to 4405 cal. yrs BP. The second larger hearth was dated to 2915 cal. yrs BP. The two other rust levels above were dated to 2600 and 2545 cal. yrs BP. Both hearths were considered to represent sporadically occupied campsites. Nevertheless, they allowed determination of the ages of the rust and albic patterns at the same burial levels. The evidence of spodic horizons is thus older than 2600 cal. yrs BP. In the sediments, erosion of the spodic Bh horizons, followed by the Bs horizons was recorded after 2600 cal. yrs BP, which is consistent with the absence of these horizons in the soils after 2600 cal. BP. Dates obtained from potential old spodic levels in PSB1 that range from approximately 3000 and 2600 cal. yrs BP are also consistent with dates obtained from a Podzol by [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF] at an elevation of 1940 m. Moreover, two other profiles at 2000 m on the Italian side of the pass (La Thuile/Plan Veyle Verney 3-2000 m and La Thuile/Plan Veyle Verney 2-2004 m) also contain hearths and albic levels that are contemporary with the recorded human activities [START_REF] Rey | Approche d'un territoire de montagne: occupations humaines et contexte pédo-sédimentaire des versants du col du Petit-Saint-Bernard, de la Préhistoire à l'Antiquité[END_REF]. Thus, the stagnic horizons seem to be more recent than the spodic horizons, suggesting that hydromorphic processes began to dominate the Podzolization. A Roman tile found in the albic horizon of a current Stagnosol (Col du Petit Saint-Bernard -Sondage 14) confirms this trend [START_REF] Rey | Occupations et circulations pré-romaines autour du Col du Petit-Saint-Bernard; méthode et premiers résultats d'une étude archéologique et sédimentaire de la montagne alpine[END_REF].

Pedo-landscape evolution around the Petit Saint-Bernard Pass and implication for the evolution of the ecosystem cycle

Following glacier retreat and lake formation, Cambisols are expected to have quickly developed and acidified in the area of the pass, helped by the growth of vegetation, particularly by Pinus cembra (Fig. 8a-b-c). On the steeper slopes, colluvial movement of soils may have regularly rejuvenated these Cambisols, as seen in VERS3 (Figs. 2 and8e). Furthermore, within the upper part of the catchment, pedogenesis was likely slower, due to the sparser vegetation, longer periods of snow cover, steeper slopes and rock landslides that are found there. Thus, only weakly differentiated profiles are found in the western part of the catchment of Lake Verney, as reported by [START_REF] Talon | Analyses anthracologiques au col du Petit St-Bernard. Archéoanthracologie et pédoanthracologie[END_REF]. As a consequence, Regosols and Cambisols were present in the landscape throughout the Holocene, though they may have been more strongly represented in the landscape before podzolization (Fig. 8-a-b-c).

The process of Podzolization seems to have progressed after 10,000 cal. yrs BP and likely reached its maximum between 6000 and 4000 cal. yrs BP . Following the beginning of human activities at approximately 4300 cal. yrs BP, changes in vegetation cover that were associated with an increase in erosion disrupted the soils that were present in the area of the pass. First, between 4300 and 2600 cal. yrs BP, soil litter and organic surface horizons were eroded, followed by the eluvial horizons of Podzols and parts of the spodic horizons between 2600 and 1000 cal. yrs BP (Fig. 8-h-i). A current analog was described by [START_REF] Pallmann | Pédologie et Phytosociologie[END_REF], who reported that, following thinning of a Pinus cembra forest, the settlement of grass and pasture led to a rapid degradation of acid humus horizons, transforming Podzols into poorly developed Podzols, grazing triggering a regression in soil evolution, and mixing the previously well-defined horizons.

As erosion increased, the spodic horizons came to the surface and mineralized, forming amorphous compounds. These compounds could be mobilized and transported or they could be covered with new materials (spodic or other) from upper parts of the slope (Fig. 8-h-i-j). In some cases, as PSB4, erosion deposited material that buried the former soils, consequently forming paleosols (Figs. 2 and 8-g) In the upper part of PSB2, regular inputs of coarse elements, slightly weathered, associated with higher pH of 8 would have led to the prevention of Fe migration and the differentiation of rust and albic horizons (Figs. 2 and8-i). Regular deposits are much easier to mobilize than the fine material generated from calcareous schists which is prone to solifluction, generating humps and hollows [START_REF] Legros | Soils of Alpine mountains[END_REF].

Archaeological evidence, such as the hearths noted in PSB1 (Fig. 8h) or the piece of Roman tile found in Séez/Col du Petit Saint-Bernard -Sondage 14 (Fig. 8-j) are sometimes found between two levels of deposits. A new deposit is then emplaced producing new material for pedogenesis that dissociates between rust and albic levels due to the presence of vegetation. Indeed, change in litter, and new hydrological conditions in the soils of the catchment can prevent podzolization. Modification of hydrological conditions associated with pedogenetic change occurred due to the change in vegetation from native forest to land clearing [START_REF] Willis | Does soil change cause vegetation change or vice versa? A temporal perspective from Hungary[END_REF][START_REF] Mourier | Soil evolution and subalpine ecosystem changes in the French Alps inferred from geochemical analysis of lacustrine sediments[END_REF] but also due to the long use of the pasture over millennia and the possible development of irrigation in the area of the pass [START_REF] Rey | Réservoirs et systèmes d'irrigation dans les alpages du col du Petit Saint Bernard: vers l'identification de structures antiques[END_REF]. Indeed, hydrological changes such as drainage can led to rapid changes in soil properties [START_REF] Montagne | Changes in the pathway and the intensity of albic material genesis: role of agricultural practices[END_REF]. Several authors have described the degradation of Podzols, but mainly in term of evolution into Cambisols [START_REF] Dambrine | Contribution à l'étude de la répartition et du fonctionnement des sols de haute montagne: massifs des Aiguilles Rouges et du Mont-Blanc[END_REF][START_REF] Willis | Does soil change cause vegetation change or vice versa? A temporal perspective from Hungary[END_REF][START_REF] Mourier | Distinguishing subalpine soil types using extractible Al and Fe fractions and REE geochemistry[END_REF][START_REF] Poulenard | Organic geochemistry of soils and sediments: a key to describe the anthropocene? In: Collection EDYTEM -Sols et Matières Organiques: Mémoires et Héritages[END_REF]. For example, [START_REF] Dambrine | Contribution à l'étude de la répartition et du fonctionnement des sols de haute montagne: massifs des Aiguilles Rouges et du Mont-Blanc[END_REF] described the degradation of Podzols into Cambisols I in response of the spread of agriculture into altitude pasturelands. The climate-specific conditions of the Petit Saint-Bernard Pass and the possible initially hydromorphic properties of the Podzols could have prevented from their development into Cambisols.

In the Middle Ages, the changes in the composition of herds, from primarily sheep to cows and/or the intensification of pastoralism appear to have been responsible for both the intensification of erosion and the acceleration of hydromorphic processes. Cattle can compact soils and cause increased runoff [START_REF] Trimble | The cow as a geomorphic agent-a critical review[END_REF], changing the susceptibility of soils to water erosion [START_REF] Giguet-Covex | Changes in erosion patterns during the Holocene in a currently treeless subalpine catchment inferred from lake sediment geochemistry (Lake Anterne, 2063 m a.s.l., NW French Alps): the role of climate and human activities[END_REF][START_REF] Brisset | The overlooked human influence in historic and prehistoric floods in the European Alps[END_REF]. However, the depletion of soils in organic matter, due to the degradation of Podzols and the development of Stagnosols can also be responsible for degradation of the soil structure [START_REF] Oldeman | The Global Extent of Soil Degradation[END_REF], and this process can accentuate erosion without any change in pasture intensity as a possible feedback process [START_REF] Yaalon | Framework for man-made soil changes-an outline of metapedogenesis[END_REF].

To established a general model of soil evolution trajectories, we replace the soil evolution of the Petit Saint Bernard pass area in the ecosystem cycle evolution described by [START_REF] Holling | The resilience of terrestrial ecosystems: local surprise and global change[END_REF] and adapted for soil cycle functioning by [START_REF] Poulenard | Organic geochemistry of soils and sediments: a key to describe the anthropocene? In: Collection EDYTEM -Sols et Matières Organiques: Mémoires et Héritages[END_REF] (Fig. 9). The cycle is made up of 2 axes that correspond to Capital versus Connectedness and organization which were adapted to Stock and Fluxes for the soil system [START_REF] Poulenard | Organic geochemistry of soils and sediments: a key to describe the anthropocene? In: Collection EDYTEM -Sols et Matières Organiques: Mémoires et Héritages[END_REF]. We choose to address organic carbon here because it appears relevant for the evolution of soils in the Petit Saint-Bernard Pass area, because it can help distinguish e.g., Podzols from Stagnosols, as well as the different horizons of Podzols, and because it is a key constituent that is necessary for soil ecosystem services. Both axes are controlled by the soil-forming factors [START_REF] Jenny | Factors of Soil Formation--a Sytem of Quantitative Pedology[END_REF], of which we emphasize the Human effect as a major soil-forming factor [START_REF] Yaalon | Framework for man-made soil changes-an outline of metapedogenesis[END_REF][START_REF] Richter | Humanity's transformation of Earth's soil: Pedology's new frontier[END_REF]. However, its presence as an individual factor is questionable because of its ability to change all the others. The third axis which accounts for parent material (p) and relief (r), represents the spatial dimension and the diversity of the pedo-landscape. The cycle begins with a phase of rapid soil growth (R), following glacial retreat and the formation of Leptosols and Cambisols, as described in the early Holocene soil evolution (Figs. 8 and9). The soils reach a relative steady state, which is defined as the conservation phase (K). The organic carbon is maximal, and this phase corresponds to the Holocene climatic optimum and the maximal expansion of both Podzols (S 1 ) and Pinus cembra forest in the subalpine area . The Ω phase is initiated in our case by the beginning of human activities and represents a phase of release, characterized by deforestation, erosion and the haploidization of soil horizons. The haploidization process was introduced to describe the mixing and/or loss of soil horizons (Fig. 9) and contrasts with horizonation [START_REF] Hole | A classification of pedoturbations and some other processes and factors of soil formation in relation to isotropism and anisotropism[END_REF][START_REF] Johnson | Evolution model of pedogenesis[END_REF]. Carbon stock decreases according to the horizons, and fluxes vary according to the intensity of the exported stock. Each single soil within the landscape follows a particular Ω trend that depends on local and temporal pressures, such as use as a campsite, overgrazing and according to the topography (the third dimension), which allows export and/or deposition of eroded material, thus multiplying the pedogenesis trajectories and increasing pedodiversity [START_REF] Ibañez | Pedodiversity: concepts and measures[END_REF]. The Ω phase is an intense, short and regressive phase that brings soils to a less developed state than they had during the K phase; and in some case to complete erosion of soils (S 0 ). The α phase constitutes a reorganization phase that is characterized by a rebalancing of the soil cover due to the existence of new environmental (i.e., hydrology, vegetation, grazing…) conditions, leading to the development of Stagnosols (S 2 ) and to the beginning of a new cycle (Fig. 9). Contrary to [START_REF] Holling | The resilience of terrestrial ecosystems: local surprise and global change[END_REF], the α phase cannot be assimilated into a new R phase because soils do not return to their initial condition and develop from the degraded, previously existing soil. [START_REF] Yaalon | Framework for man-made soil changes-an outline of metapedogenesis[END_REF] introduced the term of metapedogenesis (m i ) to indicate "the [hu]man-induced processes and changes in the soil profile". The pristine soil evolution defines the pedogenesis, and the different Ω-α trajectories of the ecosystem define the anthropo-pedogenetic phases. Thus, the soil S i + 1 (with i ≠ 0) results from the anthropo-pedogenesis m i applied to S i and so on: S i + 1 = f(S i , m i ). The Ω-α trajectories are directly involved in the provision of ecosystem services from the soil's natural capital [START_REF] Dominati | A framework for classifying and quantifying the natural capital and ecosystem services of soils[END_REF], and permit quantification and valuation of the ecosystem services provided by pasture soils [START_REF] Dominati | A soil change-based methodology for the quantification and valuation of ecosystem services from agro-ecosystems: a case study of pastoral agriculture in New Zealand[END_REF].

Conclusion

The study of the Holocene sediment sequence of Lake Verney and the analysis of current pedogenesis in the area of the Petit Saint-Bernard Pass allowed us to reconstruct the evolution of past soil processes in relation to past human activities. According to the substantial content of carbonate material in the sediment, decarbonatation seems to have been the main process that occurred during the first part of the Holocene. The acidification of the soils due to the presence of Pinus cembra vegetation and the increase in the Fe Ox /Fe Tot ratio until 6000 cal. yrs BP indicate the formation and migration of Fe organometallic compounds allowed the podzolization of the soils within the catchment during the mid-Holocene period. The beginning of human activities was recorded at 4300 cal. yrs BP, and was associated with land clearing and the successive erosion of the surface of Podzols horizons. During the Roman period, the spodic horizons were stripped away, meanwhile, erosion increased in response to sheep grazing. During the Middle Ages, pasturing way to cattle farming. Erosion increased again while the Fe Ox /Fe Tot ratio decreased, suggesting that the Podzols evolved into Stagnosols since that time. The study of paleosols, archaeological evidence and charcoal dating from soils in the area of the pass allowed validation of the soil evolution reconstruction from the lake sediment archive. The paleosols also confirmed the development of Stagnosols from degraded spodic horizons and provide additional information on erosional processes and the chronology of the Anthropocene. The combined studies of lake sediment archives and paleosols provide a long-term continuous reconstruction of pedogenesis at the landscape scale. Our study highlights the effect of the human soilforming factor in the soil cycle evolution, and provides evidence of "anthropo-pedogenetic" phases. More than changes in vegetation and agro-pastoral activities, it is more the continuous use and progressive degradation of the soil cover that lead to soil changes. The change in soil type from Podzols to Stagnosols leads to reduced accumulation of organic matter that may have consequences for both the soil structure, favoring erosion, and carbon sequestration. This understanding of "release-reorganization" trajectories, i.e., the anthropo-pedogenesis, could provide a possible means to quantify and value long-term soil ecosystem services. [START_REF] Holling | The resilience of terrestrial ecosystems: local surprise and global change[END_REF] to pedogenesis cycles and conceptual framework for man-made soil changes of [START_REF] Yaalon | Framework for man-made soil changes-an outline of metapedogenesis[END_REF] applied to soil evolution in the Petit Saint Bernard Pass area. R corresponds to the rapid growth of soil, K to the conservation phase, Ω to the release phase and α to reorganization. Gray cycles in the background represent the diversity of the pedo-landscape according to the r and p factors [START_REF] Jenny | Factors of Soil Formation--a Sytem of Quantitative Pedology[END_REF]. Doted cycles represent future cycle trajectories. The intervals between arrowheads represent the speed, i.e., a short interval means a slow change whereas a long interval indicates a rapid change. Abbreviations: C = carbon, Cl = climate, O = organism, H = human, r = relief, p = parent material, t = time, Si = soil i, mi = metapedogenetic phase i.

Leptosols

Fig. 1 .

 1 Fig. 1. Location of Petit Saint Bernard Pass (a), pictures of the Lake Verney catchment (b), locations of sampling sites and a simplified geologic map covering the area of the pass (c). Abbreviations: LTH = La Thuile.

  a -CURRENT PEDOGENESIS IN THE AREA OF THE PETIT SAINT BERNARD PASS

Fig. 2 .

 2 Fig.2. Analyses of soils in the Petit Saint Bernard Pass area according to present (A) and past (B) pedogenesis. Organic matter (OM) contents, pH, Fe contents extracted using oxalate and pyrophosphate solutions, normalized ratios of extracted Fe to total Fe, and SiO 2 /TiO 2 and Fe 2 O 3 /Al 2 O 3 ratios are shown according to depth. Photos and descriptions by P-J Rey and B. Moulin.

FeFig. 3 .Fig. 4 .

 34 Fig. 3. Correlation circles and biplots of Dimensions 1 and 2 of the principal component analysis applied to data from the soil samples including paleosols (A), 1-cm-thick sediment samples (B) and 3-cm-thick sediment samples (C). Rust and Albic samples are horizons of Stagnosols, Bh-Bs are spodic horizons of Podzols, O are organic-rich horizons, A-B are poorly differentiated brown horizons and C samples are horizons of weathered rock. Numbers in the biplots shown in (B) and (C) represent the ages of the sediment samples. SR = sedimentation rate, hz = horizons.

Fig. 5 .

 5 Fig.5. Age-depth model of the Lake Verney sediment sequence based on 14 C (A) and 210 Pb/ 137 Cs ages (B). Uncertainties are included in the dots representing 137 Cs activity measurements. The Pb/Ti ratios enable comparison of the model with the Pb emissions during modern, Medieval and Roman periods.

Fig. 7 .

 7 Fig. 7. Identification scheme of the horizon signatures of Podzols and Stagnosols in lake sediments from SiO 2 /TiO 2 , Fe Tot /Al Tot , Fe Ox /Fe Tot and Al Ox /Al Tot ratios. The Al and Fe-organometallic complexes that characterize the spodic horizons of Podzols were extracted with the acid ammonium oxalate solution. Hz = horizon, Ox = oxalate, Pyr = pyrophosphate.

Fig. 8 .

 8 Fig. 8. Reconstruction of the pedo-landscape evolution in the Petit Saint Bernard Pass area (2188 m) throughout the Holocene. a) represents the colluvial trajectories, b) represents the podzolization trajectories, c) represents the burying of Podzols by colluvial material, d) represents the evolution of the Podzol type soil with hearths and colluvial deposits, e) represents the general case of the development of stagnic properties from Podzols and f) represents an archaeological case of the development of stagnic properties (Rey and Moulin, 2006).

Fig. 9 .

 9 Fig.9. Adaptation of the ecosystem evolution model of[START_REF] Holling | The resilience of terrestrial ecosystems: local surprise and global change[END_REF] to pedogenesis cycles and conceptual framework for man-made soil changes of[START_REF] Yaalon | Framework for man-made soil changes-an outline of metapedogenesis[END_REF] applied to soil evolution in the Petit Saint Bernard Pass area. R corresponds to the rapid growth of soil, K to the conservation phase, Ω to the release phase and α to reorganization. Gray cycles in the background represent the diversity of the pedo-landscape according to the r and p factors[START_REF] Jenny | Factors of Soil Formation--a Sytem of Quantitative Pedology[END_REF]. Doted cycles represent future cycle trajectories. The intervals between arrowheads represent the speed, i.e., a short interval means a slow change whereas a long interval indicates a rapid change. Abbreviations: C = carbon, Cl = climate, O = organism, H = human, r = relief, p = parent material, t = time, Si = soil i, mi = metapedogenetic phase i.

Table 1

 1 Radiocarbon ages for Lake Verney sediment sequence.

	Sample name	Lab. code	Depth (mm)	Sample type	Age (BP)	Min. age (cal. BP)	Max. age (cal. BP)
	VERNEY1	Poz-73372	393	Wood and twigs	8000 ± 50	8656	9010
	VER13-1	SacA 38343	548	Plant macroremains	875 ± 30	726	907
	VERNEY2	Poz-73373	753	Herbs, twigs and moss	4615 ± 35	5145	5465
	VER13-02A-88	SacA 32338	1048	Plant macroremains	2100 ± 35	1989	2287
	VERNEY3	Poz-73374	1213	Herbs, twigs and moss	3350 ± 35	3481	3687
	VERNEY4	Poz-73375	1353	Herbs, twigs and moss	3940 ± 50	4241	4521
	VER13-02B-61	SacA 32339	1748	Plant macroremains	8890 ± 45	9793	10,188
	VER13-02B-96	SacA 32340	2108	Plant macroremains	9725 ± 50	10,876	11,240
	VER13-3	SacA 38345	2383	Plant macroremains	9780 ± 60	10,905	11,315
	Bold samples correspond to excluded dates from age-depth modeling.

  Geoderma 306 (2017) [217][218][219][220][221][222][223][224][225][226][227][228][229][230][231][232][233][234][235][236] contents of Fe Ox and display variations in Fe 2 O 3 /Al 2 O 3 and SiO 2 /TiO 2 ratios, similar to those seen in the Podzols. PSB2 was covered by a succession of coarse colluvial deposits over approximately 40 cm in thickness. PSB1 includes two hearths at depth of 40 and 50 cm that have been dated using Pinus charcoals to 2915 and 4405 cal. yrs BP, respectively

		% Extracted-Fe	Extracted-Fe / Fe Tot	SiO 2 /TiO 2
																				Fe 2 O 3 /Al 2 O 3
		% Extracted-Fe	Extracted-Fe / Fe Tot	SiO 2 /TiO 2
	0
	2545 cal. BP
	2600 cal. BP
	2915 cal. BP
	4405 cal. BP
	4705 cal. BP
	4725 cal. BP
	m
	c 0 7																			Fe 2 O 3 /Al 2 O 3
	COLLUVIC PALEOSOLS	%	E	t x	a r	t c	d e	F -	e	E	x	r t	a	c	d e t	-	e F	/	F	e Tot
																				Fe 2 O 3 /Al 2 O 3

(caption on next page) M.

Bajard et al.

Acknowledgments

The authors thank the city of La Thuile in Italy (Roberto Maddalena and Barbara Frigo) for access and coring authorizations and the ski resort of La Rosière for the winter access to the lake by the ski slopes. Thanks to Stéphanie Thiebault and Claire Delhon for charcoals identification of PSB1, Julie Deyrieux for the sedimentological analyses, Aurélien Borgeat, Manu Mallet and Pierre Faivre for field support. Thanks also to Sarah Bureau for ICP-AES analyses at ISTerre laboratory and to Delphine Rioux from LECA laboratory for DNA sampling and analyses. 14C analyses were acquired thanks to the CNRS-INSU ARTEMIS national radiocarbon AMS measurement program at Laboratoire de Mesure du 14C (LMC14) in the CEA Institute at Saclay (French Atomic Energy Commission). The authors thank also the Laboratoire Souterrain de Modane (LSM) facilities for the gamma spectrometry measurements. This research was performed by Hannibal Project financed by the DIPEE (Dispositifs de Partenariat en Ecologie et Environnement) Chambéry-Grenoble of the CNRS INEE.