La Formation de Waziers est constituée d'un dépôt alluvial limoneux surmonté de tuf calcaire et de tourbe. Elle est conservée dans un petit paléo-chenal de la rivière Scarpe-Scarbus, reconnu sur plusieurs centaines de mètres de long à l'entrée de la plaine de la Scarpe et daté de la fin du Saalien (SIM 6) et de l'Eemien (SIM 5e). La Formation de Waziers a été préservée à la faveur d'une défluviation ultérieure à son dépôt puis de son scellement par des dépôts fluvio-éoliens de la fin du Pléniglaciaire weichselien (SIM 2). La synthèse de l'ensemble des données et études (lithologie, paléontologie, géochronologie, reconstitution des paléotem- pératures) fournit une image cohérente de l'évolution de la zone depuis la fin du Saalien vers 130 000 ans environ jusqu'à la fin du Pléniglaciaire weichselien. À la base, les alluvions sablo-graveleuses (témoignant d'écoulements dynamiques) puis limoneuses (Membre 1) se déposent dans le fond de vallée à la fin du glaciaire saalien dans un contexte d'amorce de reconquête forestière. Un plan d'eau se développe ensuite, permettant le dépôt d'une craie lacustre dans un marais à Characées puis d'une tourbière (Membre 2, env. 1,5 m d'épaisseur) dans un contexte forestier. Un cours d'eau chenalisé circule encore dans la tourbière, au moins par intermittence, érodant et déposant localement des alluvions limoneuses. La partie inférieure du Membre 2 enregistre la transition du glaciaire Saalien (fin SIM 6) à l'Interglaciaire eemien (début SIM 5e) dans un contexte de sédimentation continue de plus en plus organique. La partie supérieure du Membre 2 enregistre l'optimum climatique eemien dans un faciès de tourbe typique, puis l'amorce d'une dégradation climatique. Au toit du Membre 2 (et celui de la Formation) est observée la limite d'une érosion majeure qui n'a pas permis l'enregistrement de la fin de l'Interglaciaire eemien. À la base du Membre 3 (env. 3 m d'épaisseur), des écoule- ments concentrés dans des ravines profondes sur sol gelé démantèlent et remanient les dépôts sous-jacents. Ensuite, des écoulements (attribués au Pléniglaciaire weichselien) déposent une nappe de graviers de craie sur l'ensemble du site dans une bande active plus large (probable tressage). La majeure partie du Membre 3 est constituée de dépôts limono-sableux fluvio-éoliens et d'un mince dépôt loessique terminal. La qualité de l'enregistrement sédimentaire de la formation de Waziers, avec notamment un dépôt continu au moment de la transition climatique du Saalien à l'Eemien, et l'abondance des éléments paléontologiques (bois et macrorestes végétaux, macro et méso-faune, microfaune, avifaune, malacofaune…) dans les dépôts eemiens font de celle-ci un témoin exceptionnel pour les recons- titutions paléoenvironnementales et paléoclimatiques de cette période. La présence de niveaux témoignant d'occupations humaines récurrentes dans les Membres 1 et 2 (éclats isolés, amas de débitage, traces d'actions anthropiques sur faune) font de ce site et de cette séquence une référence pour la compréhension des dynamiques de peuplement humain entre le SIM 6 (Saalien) et le SIM 5e (Eemien) dans le Nord de la France et plus largement dans le Nord-Ouest de l'Europe.

The Waziers Formation consists of a silty alluvial deposit topped by calcareous tuff and peat. It is preserved in a small palaeo-channel of the Scarpe-Scarbus river, recognised over several hundred metres long at the edge/entrance of the Scarpe river plain and dated to the end of the Saalian (SIM 6) and the Eemian (SIM 5e). The Waziers Formation was preserved by a later defluviation and the sealing by fluvio-aeolian deposits of the late Weichselian Pleniglacial (SIM 2). The synthesis of all the data and studies (lithology, palaeontology, geochronology, reconstruction of palaeotemperatures) provides a coherent picture of the evolution of the area since the end of the Saalian around 130,000 years ago to the end of the Weichselian Pleniglacial. At the base, sandy-gravelly (indicating dynamic flows) and then silty alluvium (Member 1) was deposited in the valley bottom at the end of the Saalian glacial period in a context of incipient forest reconquest. A water body then develops, allowing the sedimentation of a lacustrine chalk deposited in a Characeae marsh, followed by a peat bog (Member 2, ca. 1.5 m thick) in a forest context. A channelled stream still flows through the bog, at least intermittently, locally eroding and depositing silty alluvium. The lower part of Member 2 records the transition from the Saalian glacial (end of MIS 6) to the Eemian interglacial (beginning of MIS 5) in a context of continuous sedimentation with increasing organic content. The upper part of Member 2 records the Eemian climatic optimum in a typical peat facies, followed by the onset of climatic degradation. At the top of Member 2 (and that of the Formation) is the limit of a major erosion that did not allow the recording of the end of the Eemian interglacial. At the base of Member 3 (ca. 3 m thick) flows concentrated in deep gullies on frozen ground dismantle and rework the underlying deposits. Subsequently, flows (attributed to the Weichselian Pleniglacial) deposit a sheet of chalk gravels over the whole site in a wider active band (likely braiding). Most of Member 3 consists of fluvio-aeolian silty-sandy deposits and a thin terminal loessic deposit. The quality of the sedimentary record, with in particular continuous depo-sition at the time of the climatic transition from the Saalien to the Eemian, and the abundance of palaeontological elements (wood and plant macro-remains, macro-and meso-fauna, microfauna, avifauna, malacofauna...) in the Eemian deposits ensure the Waziers Formation is an exceptional testimony for the palaeoenvironmental and palaeoclimatic reconstructions. The presence of levels testying to recurrent human occupations in Members 1 and 2 (with isolated flakes, heaps of debitage, traces of anthropic actions on fauna) make this site and sequence a reference for the understanding of the human settlement dynamics from the MIS 6 (Saalian) to the MIS 5e (Eemian) in Northern France but also broadly in North-Western Europe.

Les jeux de données présentés ci-après sont issus des recherches menées sur le gisement de Waziers le Bas-Terroir depuis 2013 (Hérisson et al., 2022, pour les détails des recherches et opérations de terrain). Le présent data paper vise donc à mettre à disposition de la communauté scientifique des données brutes ou complémentaires à celles présentées au sein des articles des tomes 1 et 2 consacrés au gisement eemien de Waziers le Bas-Terroir, à savoir les numéros 33-4 (2022) et 34-1 (2023) de la revue Quaternaire. Les données (hormis le set de données n°5) sont stockées au sein de l'entrepôt de données de recherche pour les Sciences Humaines et Sociales Nakala. Les données de Nakala sont stockées sur des serveurs gérés par Huma-Num, au centre de calcul de l'IN2P3 en France. Toutes les données du présent data paper sont regroupées au sein d'une collection intitulée « Waziers le Bas‑Terroir tome 1 & 2 Data paper revue Quaternaire » et accessible via le DOI 10.34847/nkl.de671e05 ou via le DOI indiqué pour chaque fichier dans le data paper. Le set de données n°5 a été déposé sur la plateforme PRIDE (PRoteomics IDEntifications Database). Les fichiers sont mis à disposition sous une licence Creative Commons Attribution Non Commercial No Derivates 4.0 International (CC-BY- NC-ND-4.0).

The present dataset comes from rechearch led on the Waziers le Bas-Terroir site since 2013 (Herisson et al., 2022, for details about the research and fieldwork). The present data paper aims to share with the scientific community the raw or supplementary data to those presented in the papers of the volume 1 and 2 dedicated to Waziers le Bas-Terroir eemian site, corresponding to volumes 33-4 (2022) et 34-1 (2023) of Quaternaire. Data (except for data set #5) is stored in the Research Data Warehouse for Human and Social Sciences called Nakala. Nakala data is stored on servers managed by Huma-Num, at the IN2P3 data centre in France. All data in this data paper are grouped in a collection entitled << Waziers le Bas-Terroir tome 1 & 2 Data paper revue Quaternaire >> and accessible through the DOI 10.34847/nkl.de671e05 or through the DOI indicated for each file in the data paper. Data set #5 has been deposited on the PRIDE platform PRIDE (PRoteomics IDEntifications Database). The files are provided under a licence Creative Commons Attribution Non Commercial No Derivates 4.0 International (CC-BY-NC-ND-4.0).

The Last Interglacial (LIG or Marine Isotopic Substage 5.5, MIS5.5), which is comprised between similar to 129 and similar to 116 thousand years Before Present (hereafter ky BP), is poorly documented, especially in continental areas, owing to the scarcity of deposits attributable to this period, which corresponds to the Eemian in the chronostratigraphy of northwestern Europe. The scarcity of documentation is even more pronounced for the deglaciation that precedes the LIG, the MIS 6/5 Transition or Termination 2, which lasted about ten thousand years. In this context, the site of Waziers, in Western Europe (France), has an exceptional sequence of successive fine silty-limestone deposits covering the penultimate deglaciation (MIS 6/5) and peat rich in plant remains contemporary with the last interglacial (MIS 5.5). Oxygen isotope analysis of phosphate of tooth enamel from large herbivorous mammals (horse, Equus sp.; megaloceros, Megaloceros giganteus; roe deer, Capreolus capreolus) present in these deposits allows the reconstruction of air paleotemperatures during the lifetime of the animals. The results yield annual mean temperatures of 4.7 +/- 0.6 degrees C for an early phase of the deglaciation (5 teeth of a same individual), of 6.9 +/- 0.5 degrees C for a mid-phase of the deglaciation (1 tooth), and of 8.6 +/- 0.5 degrees C for a phase preceding the establishment of the last interglacial, the MIS5.5 (1 tooth). In deposits contemporary with the latter phase, human artifacts were discovered, as well as in those of MIS5.5. In agreement with the palynological data, the paleotemperatures illustrate a gradual warming during part of the glacial/interglacial transition, the MIS6/5 Transition. The difference of similar to 4 degrees C between the minimal and maximal temperature reconstructed in this study allows us to minimize the temperature difference between the MIS6.2 glacial period and the MIS5.5 interglacial period at the Waziers site.

In the context of climate change, authorities must take actions for adapting to local impacts. However, one can notice that they have difficulties doing so. In this study, we aim at identifying the obstacles to action, or on the contrary, what can be levers for adaptation. We investigated mid altitude mountains at mid latitudes in the French Alps (western Europe), where the impacts of climate change are already clear. A double survey has been realized with authorities over the French region Auvergne Rhône-Alpes, for observing their perception of levers and obstacles for adaptation at local scale. Nuancing literature, the results states that the failure to bring action at local scale is not necessarily due to a weak awareness of climate change impacts, but rather to uncertainties in i) possible futures of climate and territories, ii) knowledge brokering on global changes and their local impacts and iii) relevance of actions undertaken. Interviewees, local actors directly involved into the definition of adaptation strategies, reveal a need of places for dialogue and sharing of experiences on adaptation, but also a need for guidance to initiate major changes toward reducing vulnerabilities of mid altitude mountains.

La dernière période interglaciaire (Last Interglacial, LIG, ou Stade Isotopique Marin 5.5, SIM 5.5), comprise entre environs 129 et environs 16 milliers d'années avant aujourd'hui (ci-dessous ka), est peu documentée, en particulier en domaine continental en raison de la rareté des dépôts attribuables à cette période qui correspond à l'Eemien dans la chronostratigraphie de l'Europe du nord-ouest. Le manque de documentation est encore plus prononcé pour la déglaciation qui précède le LIG, la Transition SIM 6/5 ou Terminaison 2, qui a duré une dizaine de milliers d'années. Dans ce contexte, le site de Waziers, localisé en Europe occidentale (France), présente une séquence exceptionnelle constituée de dépôts successifs fins limono-calcaires couvrant l'avant-dernière déglaciation (SIM 6/5) et des tourbes riches en restes végétaux contemporaines du dernier interglaciaire (SIM 5.5). L'analyse isotopique de l'oxygène du phosphate de l'émail de dents de grands mammifères herbivores (cheval, Equus sp. ; mégalocéros, Megaloceros giganteus ; chevreuil, Capreolus capreolus) présents dans ces dépôts a permis de reconstituer les paléotempératures de l'air du vivant des animaux. Les résultats donnent des températures moyennes annuelles de 4,7 ± 0,6°C pour une première phase de la déglaciation (5 dents d'un même individu), de 6,9 ± 0,5°C pour une phase médiane de la déglaciation (1 dent), et de 8,6 ± 0,5°C pour une phase précédant l'établissement du dernier interglaciaire, le SIM 5.5 (1 dent). Des artefacts paléolithiques (silex) ont été découverts dans les dépôts contemporains de cette dernière phase - ainsi que dans ceux attribués au SIM 5.5. En accord avec les données palyno- logiques, les paléotempératures mettent en évidence un réchauffement progressif au cours d'une partie de la transition glaciaire/ interglaciaire, la Transition SIM 6/5. L'écart de environ 4°C entre la température minimale et la température maximale reconstituées ici permet de minorer l'écart de température entre la période glaciaire SIM 6.2 et la période interglaciaire SIM 5.5 sur le site de Waziers.

The hard and soft tissue remains of a pre-Hispanic population of the Gran Canaria Island at six different archaeological localities were studied using C-14 dating and stable isotope compositions. Radiocarbon dating indicates island occupation ranging from the beginning of the 7th to the mid-14th century. We analyzed the oxygen isotope compositions of apatite phosphate bones of some pre-Hispanic individuals. The oxygen isotope compositions of meteoric water (delta O-18(w)) show a significant decrease from -2.1 +/- 1.5 to-4.4 +/- 1.2 parts per thousand (VSMOW) from the Medieval Warm Period (MWP) to the Little Ice Age (LIA). This is interpreted to reflect a decrease in air temperature by about 5 +/- 3 degrees C. Archaeological data along with delta C-13, delta N-15 and delta S-34 values of soft tissue indicate that the pre-Hispanic population from Gran Canaria relied on agriculture throughout the 7th to mid-14th century. However, a significant contribution of seafood to the diet of the pre-Hispanic population is observed at archaeological sites located close to the shore. These results suggest cultural resilience in the pre-Hispanic population of Gran Canaria, reflected in the relative constancy of their diet in light of climate change.

The Canary Islands, east of the North Atlantic Ocean (27 degrees N-29 degrees N), are under the influence of the Canary Current, the descending branch of the North Atlantic Gyre, which is modulated by coastal upwelling off North-West Africa. They constitute strategic sites for palaeoclimatic reconstructions, especially for the Last Interglacial (LIG, 129 to 116 ky BP) estimated to be warmer than present. Seventy-four carbon and oxygen isotope bulk analyses and time series measurements were performed on 32 aragonitic mollusc shells from the LIG marine deposits on Lanzarote and Fuerteventura islands during a period of sea-level highstand that we estimated to occur between approximate to 125 and 119-116 ky BP. Our SST calculations, inferred from shell delta O-18 values using available isotopic fractionation equations, provide a seasonal SST amplitude ranging from 3.5 degrees C to 6.0 degrees C, in agreement with the modern seasonal amplitude, along with a mean SST comprised between 20.4 +/- 1.3 degrees C and 22.2 +/- 1.2 degrees C. With respect to the pre-industrial times, we deduce a positive SST anomaly in the range of +1.0 +/- 1.4 degrees C to +2.8 +/- 1.3 degrees C, consistent with the presence of the species Persististrombus latus, typical of warm SSTs. Although this finding does not match with the zonal negative anomaly of a reconstructed SST at low latitudes of the North Atlantic, it is nevertheless corroborated by other climate reconstructions in the northeastern tropical Atlantic region. We attribute this trend to an excess of summer insolation during the LIG which warmed the Canary Current, enhanced by a weakening of the North African upwelling. The entire North Atlantic Gyre was probably warmer during the LIG. (C) 2020 Elsevier Ltd. All rights reserved.

Abstract The study of paleoclimates enables us to improve and better constrain climate models in order to forecast future climate variations. Marine Isotope Stage 11 (MIS11), which began around 425,000 yr BP and lasted about 65,000 yr, is a warm isotope stage of paramount importance, because the astronomical configuration was similar to the one characterizing the Holocene. Therefore, this warm isotope stage is the most appropriate analog to present-day climate known to date. This study aims to provide new data on sea-surface temperatures (SSTs) inferred from the carbon and oxygen isotope compositions of skeletal carbonates of marine invertebrates preserved in two marine deposits of the Canary Islands located at Piedra Alta, Lanzarote, and Arucas, Gran Canaria. According to published isotopic fractionation equations the marine deposit from Arucas recorded SSTs of 15.9 ± 2.2°C on average, while the tsunamite from Piedra Alta recorded SSTs of 21.2 ± 1.9°C on average. Absolute dating, mollusc assemblages, and calculated marine temperatures suggest that the Arucas marine deposit corresponds to the beginning of MIS11, while the Piedra Alta tsunamite was formed during MIS11c. These results show that low latitudes also experienced sizable SST changes during interglacial stages.

Zinc isotopes have been studied along two smelter-impacted soil profiles sampled near one of the largest Pb and Zn processing plants in Europe located in northern France, about 50km south of Lille. Mean δ66Zn values along these two soil profiles range from +0.22±0.17‰ (2σ) to +0.34±0.17‰ (2σ) at the lowest horizons and from +0.38±0.45‰ (2σ) to +0.76±0.14‰ (2σ) near the surface. The δ66Zn values in the lowest horizons of the soils are interpreted as being representative of the local geochemical background (mean value +0.31±0.38‰), whereas heavier δ66Zn values near the surface of the two soils are related to anthropogenic Zn. This anthropogenic Zn occurs in the form of franklinite (ZnFe2O4)-bearing slag grains originating from processing wastes at the smelter site and exhibiting δ66Zn values of +0.81±0.20‰ (2σ). The presence of franklinite is indicated by EXAFS analysis of the topsoil samples from both soil profiles as well as by micro-XANES analysis of the surface horizon of a third smelter-impacted soil from a distant site. These results indicate that naturally occurring Zn and smelter-derived Zn exhibit significantly different δ66Zn values, which suggests that zinc isotopes can be used to distinguish between geogenic and anthropogenic sources of Zn in smelter-impacted soils. In addition to a possible influence of additional past sources of light Zn (likely Zn-sulfides and Zn-sulfates directly emitted by the smelter), the light δ66Zn values in the surface horizons compared to smelter-derived slag materials are interpreted as resulting mainly from fractionation processes associated with biotic and/or abiotic pedological processes (Zn-bearing mineral precipitation, Zn complexation by organic matter, and plant uptake of Zn). This conclusion emphasizes the need for additional Zn isotopic studies before being able to use Zn isotopes to trace sources and pathways of this element in surface environments.

Zinc isotopic fractionation during adsorption onto a purified humic acid (PHA), an analogue of organic matter (OM), has been investigated experimentally as a function of pH. The Donnan Membrane device (DM) was used to separate Zn bound to the PHA from free Zn2+ ions in solution and allowed us to measure the isotopic ratios of free Zn2+. Below pH 6, adsorption of Zn on the PHA resulted in no measurable isotopic fractionation, while at higher pH, Zn bound to PHA was heavier than free Zn2+ (delta66Zn(PHA-FreeZn2+) = +0.24 per thousand +/- 0.06 2sigma, n = 4). This can be explained by changes in Zn speciation with pH, with higher complexation constants and shorter bond lengths for Zn-PHA complex compared to the free Zn2+. Complexation of Zn with PHA occurred mostly through binding to high affinity sites (HAS) and low affinity sites (LAS). Fractionation factors for 66Zn/64Zn ratios determined by mass balance calculations were equal to 1.0004 for HAS (alpha(HAS-solution)) and 1.000 for LAS (alpha(LAS-soultion)). delta66Zn(OM-FreeZn2+) should then vary according to the heterogeneous nature of the OM, because of the variable relative proportions of these two types of sites. The NICA-Donnan model, along with these fractionation factors and measured delta66Zn(TotalDissolved), was used to simulate the corresponding isotopic composition of free Zn2+ in the Seine River, France: delta66Zn(TotalDissolved-FreeZn2+) varied from +0.02 per thousand to +0.18 per thousand, depending on the HAS/LAS ratio assumed for the OM. This study allows a better understanding of Zn isotope fractionation mechanisms associated with organic mater binding.

Zn isotopic fractionation caused by sorption on 2-Lines ferrihydrite (Fh2L) and goethite was investigated to assess the role of reactions at the Fe-oxyhydroxide/water interface in changes of the isotopic distribution of Zn. Since sorption reactions are ubiquitous in Earth’s surface environments, it is important to evaluate their influence on the isotopic distribution of Zn before it can be used to track and quantify contributions of various sources and/or biogeochemical processes involving this element. Our results show that Zn isotopes are fractionated upon sorption on Fe-oxyhydroxides with an enrichment of the heavy isotopes present on the solid’s surface. This fractionation appears to proceed through an equilibrium mechanism and yields different (Δ66/64Zn)sorbed–aqueous values for Zn sorption on goethite [(Δ66/64Zn)sorbed–aqueous around +0.29‰] and Fh2L [(Δ66/64Zn)sorbed–aqueous around +0.53‰]. These different magnitudes of Zn fractionation are related to structural differences between Zn complexes existing on the surface of goethite (octahedrally coordinated Zn by oxygen atoms) and Fh2L (tetrahedrally coordinated Zn by oxygen atoms), as evidenced by Extended X-ray Absorption Fine Structure (EXAFS) spectroscopy and CD-MUSIC modeling. These results show the importance of accounting for reactions at the Fe-oxyhydroxide/water interface when dealing with the isotopic distribution of Zn at the Earth’s surface. Considering the large range of other possible sorbents (Mn or Al oxides, phyllosilicates, carbonates, biologic surfaces, etc.) and the importance of reactions at sorbent/water interfaces for other non-traditional stable isotopes (i.e. Cr, Fe, Ni and Cu) that are increasingly used in environmental studies, these results emphasize the need for further experimental studies that are needed to quantify the isotopic fractionation of these elements possibly accompanying their sorption.

The boron geochemical cycle has been simulated using a time-dependent geochemical box model that was coupled to a one-dimension model of seawater–oceanic crust interactions. Boron elemental and isotopic compositions of oceanic rocks as a function of depth were calculated by mass balance, using the temperature and porosity profiles of the crust as well as the available experimental and empirical distribution coefficients and fractionation factors between mineral and water. Ranges of boron elemental and isotopic variations of seawater were calculated for crust–seawater interactions that take place from the ridge-axis to the off-axis closure of the hydrothermal system. The present-day δ11B of seawater (40‰) could represent a steady-state value. However, depending on crustal permeability, lifetime of water–rock interactions, and expansion rate of the oceanic ridge, the δ11B of seawater may vary from 30‰ to 50‰ at the 10 million year scale.