dataesr/scientific-paragraphs-categorization huggingface dataset:
EL : Et la CBLT, elle est au quotidien avec les populations riveraines ? GM : C'est difficile à dire. Elle est impliquée dans des projets de développement, pas seulement autour du lac mais dans tout le bassin. C'est une institution lourde dont le lien avec le terrain est souvent difficile. Ça passe par des macroprojets. Il n'y a pas d'agents de la CBLT qui sont sur le terrain. Il faut avoir en tête que c'est un bassin de très grande dimension, de plus de 2 millions de km 2. CR : Ils ont de petites antennes sur le terrain mais apparaissent surtout comme maîtres d'oeuvre. Ils accueillent des projets et ce sont les projets qui déploient leurs agents sur le terrain. GM : La CBLT a un conseil scientifique et un observatoire, qui rassemblent une petite équipe avec un SIG, une gestion de base de données, etc.
Ces connaissances sont vastes et nous ne tenterons pas ici d'en couvrir la totalité. Dans la catégorie « connu connu », nous mettons en lumière les principaux messages tirés d'une revue de littérature scientifique portant sur la restauration des terres et l'adaptation sociétale au changement climatique. Nous avons interrogé la base de données SCOPUS en septembre 2018 à la recherche de travaux traitant de la restauration des terres et de l'adaptation au changement climatique, contenant le terme « restauration » uniquement dans le titre, et des termes relatifs aux écosystèmes, au climat et à l'adaptation dans le résumé, le titre ou les mots-clés. Nous sommes peut-être passés à côté de travaux pertinents, mais notre objectif était d'obtenir un aperçu des principales problématiques de la restauration en lien avec l'adaptation, plutôt que la réalisation d'une revue systématique.
Remerciements Les partenaires financiers qui ont soutenu cette étude incluent l' Initiative internationale pour le climat (IKI) du ministère fédéral allemand pour l'environnement (BMUB), l'organisme norvégien pour le développement international (NORAD) ,  le programme de financement de la recherche et de l'innovation de l'Union européenne H2020  (projet SINCERE) et le programme de recherche du CGIAR sur les forêts, les arbres et l'agroforesterie (CRP-FTA) avec l'aide financière du fonds CGIAR.
Within this frame, we investigate the tectono-metamorphic evolution of this exhumed piece of the upper crustal level of the Lesser Antilles volcanic arc. We mapped and characterized the lithologies (geochemistry, geochronology) and the structures (structural and kinematic analysis) of the Basal Complex and propose an updated geological map of this northern area of Basse-Terre. Furthermore, we accurately document its metamorphic evolution by the means of a detailed study of the metamorphic reactions preserved in the exposed lava flows and thermodynamic modeling of the mineralogical equilibrium. This dataset allows us to discuss the heat and fluid transfers in the Lesser Antilles magmatic arc, so as to propose a conceptual scheme of these transfers and their influence on the strain accommodation and metamorphic evolution, in the framework of the shallow crustal level of an active volcanic arc.
Mapping lithologies and structures With this study, we improve the geological knowledge of the Basal Complex by mapping accurately this volcanic unit, we have distinguished the following formations (see Sect. 3. 1 for a detailed description of the lithology): often very thick soils, which occupy a significant part (more than 50%) of the mapping area; superficial quaternary sedimentary formations; debris flows; lava flows. with a review of the several boundaries between the Basal Complex and the Northern Chain proposed in previous studies  (Samper et al. , 2007; Mathieu, 2010; Gailler et al. , 2013; Ricci et al. , 2015a; Barnoud et al. , 2017; Verati et al. , 2018). This study presents a structural data set consisting of about 230 measurements of bedding, fractures, faults, schistosity, and kinematic criteria acquired over 12 sites across the North of Basse-Terre Island.
Paleo stress tensors We have inversed fault kinematics with the right dihedron method to obtain the paleo-stress tensor using WinTensor software  (Angelier and Mechler, 1977; Angelier, 1979; Delvaux and Sperner, 2003). WinTensor allows rotational optimization of the obtained tensor by performing iterative tests of tensors in order to minimize a misfit function  (Delvaux and Sperner, 2003). We have performed these inversions with a dataset consisting of fault strikes, dips, plunges of the striae and kinematic criteria. For consistency, a minimum of four structural measurements (faults direction and dip, pitch and kinematics) is needed to obtain a robust paleotensor. The quality of inversion is given by QRw (world stress map quality criteria) ranging from A (very good) to E (poor quality) depending of the amount of data use for the inversion (n), the ratio between the amount of data used for the inversion over the amount of input data (n/nt), deviation between observed and theoretical slip direction (a w ), the sense of slip confidence level (Cl w ) and the type of structure (fault, fracture, shear zone).
The raw data of each step and blank were processed, and the ages were calculated using the ArArCALC software  (Koppers, 2002). Dating parameters (typical blank values, irradiation parameters and Ar-Ar analytical details) are reported in the supplementary data in Appendix (Tab. A2). The criteria for defining plateau ages are as follows: (1) Plateau steps should contain at least 50% of released 39 Ar, (2) there should be at least three successive steps in the plateau, and (3) the integrated age of the plateau should be in agreement with each apparent age of the plateau within a 2s confidence interval.
Geochemistry and petrology In order to improve the definition of the lithotypes proposed on the geological map, the magmatic characters of the lavas flows were established. Whole rock major and trace element analyses were thus realized on several samples (analytical results are provided in the supplementary data in Appendix Tabs. A3 and A4). We carefully selected the rock exposure to ensure that the main types of lava flows were sampled. We analysed rock powders by Inductively Coupled Plasma Atomic Emission Spectrometry (ICP-AES) and Inductively Coupled Mass Spectrometry (ICP-MS), for major and trace elements respectively, at the Geochemical and Petrographical Research Center in Nancy (SARM laboratory, CNRS-CRPG, with the procedure proposed by  Carignan et al. , 2001). In order to constrain and quantify the petrological evolution of the Basal Complex, we investigated 80 thin sections.
Mineral chemistry data were achieved by both electron microprobe analyses and diffractometry (system XPert-Pro MPD, Bragg Brentano geometry, Cu anticathode, KAlpha1 and KAlpha2 rays, PIXcel detector at the CEMEF in Sophia-Antipolis Scientific Center). Major elements analyses were performed at the "Service Commun de Microsonde" at Montpellier University on a Cameca-SX100 electron microprobe. The operating conditions were a 20 kV accelerating voltage and 10 nA beam current. The chemical analyses of the metamorphic phases are presented in the supplementary data in Appendix Table A5  (Schumacher, 1997). We also used Raman spectrometry to complete mineral determination (in the supplementary data, Appendix A). The spectra were recorded with a LabRam HR800UV Jobin-Yvon TM microspectrometer equipped with 1800 g/mm gratings and using 532 nm green laser excitation; acquisition time-span varied from 20 to 70 s during three accumulating cycles.
A second pattern, observed for Tillet creek samples (BT9_01-02), displays a flat-type trend with negative Ce and large positive Eu anomalies. This likely result from rock interaction with acidic high-temperature hydrothermal fluids  (Michard et al. , 1983; Michard, 1989; Cotten et al. , 1995). Multi-elements diagrams also show two different patterns (Fig. 5H ), both with Zr-Hf positive anomalies. If the first one is similar to the trends depicted in the Basal Complex volcanic rocks, another one characterizes the samples with strong negative La-Ce anomalies, negative Sr-Nd anomalies and always a large Eu anomaly. All together, these data demonstrate that the volcanic rocks of the Basal Complex were severely transformed after their crystallization in relation with hydrothermal fluid circulations and supergene alterations.
Brittle strain The Basal Complex is also affected by brittle structures. The four families of regional directions are represented on the mapped area (Fig. 6A ), with a main dominant fault family of N140-N150 (Fig. 6C ) and with centimetrical offsets. Tectoglyphs along fault planes show normal dip-slip to oblique slip kinematics at all measurements sites, except at one locality where the offset of an andesitic pebble shows an apparent inverse kinematics, although the fault plane does not display any kinematic indications. At each site and although kinematics indicators were scarce, giving weak inversion data at individual sites, paleostress inversion shows a s 3 trending NE-SW and NW-SE along N 50°and N 150°trending faults, respectively. Inversion of the whole dataset provides a pureextensional stress regime with s 3 trending NE-SW (Fig.
, 2004). Furthermore, thermodynamic calculations were performed with the free energy minimization programs THERIAK and DOMINO (De Capitani and Petrakakis, 2010; updated software v. 4 February 2017) and the internally consistent thermodynamic "tcdb55c2d" database  (Holland and Powell, 1998; updated Nov. 2003). However, thermodynamic modeling requires a strict definition of the chemical system to ensure  it corresponds to the effective bulk chemistry equilibrated during the metamorphic peak event. The previously presented geochemical data demonstrate that a significant number of the studied samples were subject to severe chemical modifications during cooling and supergene alterations. REE patterns normalized to chondrite values (Fig. 5 ) allowed the identification of the samples that were not affected by late alterations and thus that best preserved the chemical system effective during metamorphic peak conditions.
Moreover, our paleostress inversion of the whole dataset of kinematics measurements gives a pure-extensional stress regime s 3 trending NE-SW (Fig. 6D ). On the scale of the Guadeloupe archipelago with onshore and offshore investigations  (Feuillet et al. , 2002 (Feuillet et al. , , 2010 (Feuillet et al. , , 2011;; Thinon et al. , 2010; Mathieu et al. , 2011; Corsini et al. , 2011; Laigle et al. , 2013; Lardeaux et al. , 2013; Münch et al. , 2013; Leclerc et al. , 2014) , statistically, the N150-N10 structures are presented as the most recent ones, while the N40-N50 structures are the oldest in the proposed relative chronology. According to many authors, the N120-N140 structures have been synchronously activated by transtension. Finally, similar trends, observed in brittle, semi-brittle and ductile tectonic structures suggest strong inheritances within the crust of the volcanic arc of the Lesser Antilles and corroborates observations from previous workers along the Lesser Antilles volcanic arc  (Corsini et al.
Acknowledgment. This paper is a contribution to the  GEO-TREF program , funded by the  French government  with the program of " Investissements d'Avenir " and tutored by  ADEME. We thank the researchers from the  GEOTREF consortium  for greatful discussions during the fieldwork campaigns in Guadeloupe and during scientific meetings. We sincerely would like to thank the reviews, the comments and the suggestions of  Agnès Samper  and  Christoph von Hagke  that significantly improved the manuscript. The authors thank  Vivien Navelot  for his donation of some samples and geochemical data,  Matthieu Zanti  for sampling preparation,  Arthur Iemmolo  for his technical support during 40 Ar/ 39 Ar analysis and  Gabriel Monge  for his welcome to CEMEF for the use of the X-ray Diffraction device.
Pre-and post-collapse topography of the island Pre-collapse topography of Anak Island was derived from the DEMNAS (national digital elevation model of Indonesia, spatial resolution of 0. 27 arcsecond using the vertical datum EGM2008, provided by the Indonesian Geospatial Agency, and available at http://tides. big. go. id/DEMNAS/index. html). This DEM was built from InSAR, TerraSAR-X and ALOS-PALSAR data collected from 2000 to 2013. The original DEMNAS raster file was converted into a shapefile (contour lines) that was modified in order to include the latest growth of the edifice, as seen on photographs taken in August and November 2018 (http://www. oysteinlundandersen. com), and satellite images (e. g. Sentinel-2 image captured on 30 September 2018, and PlanetScope image captured on 17 December 2018: see Figure  A1 ).
Pre-collapse bathymetry is from  Deplus et al. [1995]. The contour of the collapse scar was inferred from a Sentinel-1A image captured ∼8:30 hours after the collapse (22/12/2018 at 22:33:44 UTC) and photographs taken by Susi Air flight crew the day after (23/12/2018). There is no data available on postcollapse bathymetry and the submarine extent of the collapse scar. Intense phreatomagmatic activity rising from the sea surface inside the scar produced a significant volume of pyroclastic deposits, thus reshaping the island in a few days. Post-collapse evolution of the island's perimeter could be traced from different satellite images captured between 22 December 2018 and 31 March 2019 (Sentinel-1-A/B, Sentinel-2, TerraSAR-X, PlanetScope). The topography of the island on January 10, 2019 was reconstructed using drone photogrammetry (drone footage by James Reynolds, Earth Uncut TV: https:/www.
earthuncut. tv). Images were processed using Agisoft Photoscan Pro (https:/www. agisoft. com). Using a Structure-from-Motion workflow, the software (1) detected matching points and aligned all images, (2) constructed a dense point cloud from depth information of each aligned image, (3) calculated a triangulated mesh, (4) and built a digital elevation model after 11 ground control points (GCP) were implemented (from a Sentinel 2 image captured on 13 January 2019). The resulting DEM has a resolution of 2 m per pixel, but its completeness is unequal from one flank to another due to the spatial distribution of the drone images. In order to locally complete the model, additional points were extrapolated from different aerial and ground photographs available on the web (e. g. BNPB survey of 13 January 2019).
Satellite-based SO 2 retrieval Volcanic sulphur dioxide emissions (SO 2 ) have long been characterized from satellite-based UV sensors [e. g. Schneider et al. 1999; Carn et al. 2003; Yang et al. 2007]. A variety of sensors (IR/UV) and platforms (GEO/LEO) now exists and allows a detailed description and quantification of SO 2 mass loading during eruptive events. Firstly, in this study we used the combination of Aura/OMI data (∼90 %) and Suomi-NPP/OMPS data (∼10 %) in order to capture the longterm  (195 days, between   using the "Total Column 1-orbit L2 Swath 13x24 km V003 (OMSO2)" product for OMI/Aura Sulphur Dioxide, and the "Total Column 1-Orbit L2 Swath 50x50 km" product for OMPS/NPP Sulphur Dioxide. Then, in order to better assess the eruption dynamics and provide a refined evaluation of SO 2 emissions, we processed data from the TROPOMI sensor onboard the Sentinel-5 platform.
We used the Offline timeliness L2_SO2 data products from ESA-Copernicus Pre-Operation Data-Hub (https://scihub. copernicus. eu/). For estimating SO 2 emissions before the flank collapse, we used the middle troposphere elevation model (TRM, 5-10 km) as most emissions were injected to low/moderate altitudes. By contrast, for the 22/12/2018 eruption we used the 15-km elevation model (UTLS) from TROPOMI Slant Column Densities (SCD). The calculation of the mass loadings or/and mass fluxes have already been widely described in the literature (see, e. g. Theys et al. [2013] , for a review). A variety of methods associated with satellite-based data exists, such as the Traverse, Box, Delta-M or Inverse methods. They all have their specificity and domain of application. For our study we used the box method  [Lopez et al.
g. Prata and Grant 2001 ]. Here we used TIR data from Himawari-8 (H8) geostationary satellite operated by the Japan Meteorological Agency (JMA) which provides images every 10 minutes at a spatial resolution of ∼ 2 × 2 km at nadir. Data were collected through the Centre for Environmental Remote Sensing (CEReS) using gridded data products from full-disc observation mode (http://www. cr. chibau. jp/english/database. html). The very high time resolution of TIR images used allows us to catch the dynamics of the ash plume at the initial stage, during and after the collapse (i. e. on 22/12/2018 at 13:50 UTC). In Figure  2B , we show as an example one image of the plume brightness temperature at 11. 2 µm (H8 TIR waveband #02) that allows us to determine the plume top altitude between 14 and 15 km (a.
e. mainly Strombolian). Finally, post-collapse volcanic activity emitted 173±52 kt of SO 2 in 11 days (see inset in Figure  5 ). Errors on SO 2 retrieval are difficult to assess accurately, but they can be relatively large. Indeed,  Lee et al. [2009]  have estimated in a study dedicated to validation and error analysis that the total uncertainty in the retrieval of SO 2 columns from similar instruments is in the range of 20-40 %. The flank collapse occurred on 22/12/2018 around 13:50 UTC. This has been confirmed by thermal infrared data recorded by Himawari-8 geostationary satellite (Figure  6 ), allowing the full-disc image acquisition every 10 minutes. By contrast, the TROPOMI/Sentinel-5 platform provides one image/day with an acquisition time above this region lying between 06:00 and 07:00 UTC.
Airborne ash mass and MER The amount of airborne ash emitted can also be estimated from satellite-based Thermal Infra-Red (TIR) imagery provided weather conditions are favourable. For this purpose, we used data from the geostationary platform Himawari-8 providing full-disc coverage at a 10-minutes time interval (see method section for details). From the improved split window technique using the 3-bands methods  [Guéhenneux et al. 2015] , we first detected ash-bearing pixels. Then, from inversion of TIR data using radiative transfer modelling we give the ash cloud concentration (in g m -2 ), as displayed in Figure  6 , and the airborne ash flux Q a (in kg s -1 ). From Figure  6  we observe that ash emissions can clearly be identified as early as 13:50 UTC, forming a transient high-altitude cloud of ash, coincident with the flank collapse.
, 2018)  comme celui de la Mer de Glace (données non publiées). Les méthodes d'inversion qui utilisent un modèle d'écoulement et les flux de glace  (Gilbert et al. , 2018)  ont permis de compléter la connaissance des épaisseurs de glace dans la partie haute du glacier d'Argentière, en particulier sur les affluents (glaciers des Rognons, des Améthystes et du Tour Noir) dépourvus de mesures d'épaisseur. Le lit rocheux de la partie supérieure de la Mer de Glace est beaucoup plus problématique, car il n'est connu que pour sept sections transversales dans cette zone, ce qui représente une petite partie de la zone d'accumulation. Nous avons comblé ces lacunes en utilisant la base de données  de Huss et Farinotti (2012)  qui ont utilisé une méthode basée sur un calcul de flux de glace pour estimer les lits rocheux de différents glaciers.
Huss (les glaciers un observatoire du et al. (2010) avaient également montré, à climat) (https://glacioclim. osug. fr). Cette partir d'une étude sur deux glaciers étude a été rendue possible grâce aux suisses, que les résultats entre les deux financements et données issus du projet types de modèle étaient très similaires à ANR VIP_Mont-Blanc (ANR-14-CE03- cette échelle de temps. Les formations de 0006-03) et du LabEx OSUG@2020 chutes de séracs ou de lacs proglaciaires (investissements d'avenir ANR10 à venir, comme le lac d'Argentière, LABX56). Le MNT LiDAR du glacier influenceront très probablement les d'Argentière a été acquis dans le cadre fluctuations glaciaires dans le futur, mais du projet European Facility for Airborne les impacts concerneront des périodes de Research Transnational Access (EUFAR temps de quelques années, voire d'une TA, EU FP7 Integrating Activity) -project ou deux décennies.
The Saint-Palais Unit The Saint-Palais Unit is located between the Arbailles Unit and the Saint-Palais Thrust. The The seismic line interpreted is a merger of lines MT104, MT112 and 83HBS02 (acquired by SNEAP in 1981 and reprocessed by BRGM in 2014; Fig. 10 ). The seismic interpretation was carried out using the Geographix® Discovery Suite that allows for each CDP of the seismic profile to export its X, Y, time, amplitude and depth values. Seismic/well tie is obtained by using the time / depth curves acquired in the boreholes and derived from the recording of checkshots. The time / depth conversion was performed using a mean velocity field calculated on the basis of all the time / depth data of the calibration wells, integrating their deviations (Fig. 11 ). The top basement has been calibrated taking into account the ECORS seismic reflection profile  (Daignières et al.
Acknowledgements This study was conducted within the framework of the integrated geological Orogen research project (TOTAL, BRGM, and INSU). We are very grateful to the reviewers and to the editor, who contributed to the improvement of this manuscript. We would like to thank the  Orogen project managers Sylvain Calassou (Total ),  Emmanuel Masini  (Total),  Olivier Vidal (CNRS)  and  French geological survey -BRGM. We also thank  Joseph Canérot  for the numerous scientific discussions on the tectono-sedimentary evolution of the  Mendibelza and Arbailles Units. The authors thank  Geoffrey Bird  for the English review. Canadian Journal of Earth Sciences, v. 22, no. 1, p. 108-125, doi: 10. 1139/e85-009. Wernicke, B. , and  B. C. Burchfiel ,  1982 , Modes of extensional tectonics: Journal of Structural Geology, v.
2c ). Based on sedimentological investigations and surface gamma-ray logging, the marl can be a product of background sedimentation, with occasional low-density turbidites (sand intercalations), which is a characteristic of inner fan overbank deposits as well as outer fan lobes  (Tőkés, 2013; Tőkés et al. , 2015). Based on seismic interpretation, the locality can 1000× magnification at the Department of Sedimentary Geology, Geological Survey of Austria, Vienna, Austria. Quantitative data were obtained by counting at least 300 specimens from each smear slide.
Magnetostratigraphy Guşteriţa 4 section was sampled for magnetostratigraphic purposes by drilling 26 marl samples from the quarry. Measurements were carried out in the Fort Hoofddijk Paleomagnetic Laboratory of the Utrecht University, Utrecht, the Netherlands. Magnetic susceptibility measurements were made on an AGICO MFK1-FA Multi-Function Kappabridge automatic device, using the Saphyr6 software. For the alternating field (AF) measurements, a laboratory-built automated AF-coil-interfaced measuring device with a 2G cryogenic magnetometer was used  (Mullender et al. , 2016). The following field steps were used:  0, 5, 10, 15, 20, 25, 27, 30, 32, 35, 40, 45, 50, 60 and 80  mT. The thermal (TH) measurements were carried out with a manually operated 2G Enterprises DC (ZnCl 2 , density >2. 1 kg/l) was used to separate the organic matter from the undissolved inorganic components.