dataesr/scientific-paragraphs-categorization huggingface dataset:
The pulse rate was 500 kHz with a scan angle of 45° from nadir and a swath side-lap of 50% (i. e. , almost all terrain was scanned twice from different angles). Aircraft attitude was measured by a Honeywell CUS6 IMU at a rate of 200 kHz and positional data was logged at 2 Hz using a survey-grade L1/L2 GNSS receiver mounted in the tail rotor assembly  (Evans, 2016). These data were classified into ground and nonground points using the LiForest software  (LiForest, 2016). It has been suggested that LiDAR data with point density >0. 5 pulses/m 2 produce reliable estimates of the forest canopy  (Hansen et al. , 2013)  and LiDAR data with pulse density greater than 1 pulse/m 2 have limited impact on estimating forest structure variables  (Andersen, Reutebuch, McGaughey, d'Oliveira, & Keller, 2014).
Hence, no thinning of the 2015 LiDAR dataset was carried out. Ground returns were used to derive a Digital Elevation Model (DEM) while vegetation returns were used to generate a Canopy Height Model (CHM) giving the upper boundary of the canopy  (Popescu & Zhao, 2008). The CHM and DEM were generated at a resolution of 1m  (LiForest, 2016). Furthermore, LiForest software was used for isolating individual trees from the LiDAR data and extracting their individual locations, associated tree heights and crown area  (LiForest, 2016). The individual scale LiDAR-derived tree heights were scaled to the plot scale for both 2012 and 2015  (Singh et al. , 2016). Points with elevation values greater than the height break of 2m were considered to be tree points and the ratio of LiDAR returns less than the height break to the total number of returns was computed to produce estimates of gap fractions at a 15m resolution  (LiForest, 2016).
The 2012 Landsat-LiDAR based 3 class forest cover map was found to have an overall accuracy of 98% and kappa of 0. 97 on the test data. The 2015 Landsat-LiDAR-based 3 class forest cover map was found to have an overall accuracy of 99% and kappa of 0. 98 on the test data. Analysis of these two random forest-based maps also indicated high levels of forest cover retention within the community forests. Further analysis of these data also revealed that overall forest cover declined by 20. 4% across the entire study area. This is consistent with the findings of Figure  3 , which also indicate a similar decline in forest cover values (with the Landsat-based forest-nonforest maps). Analysis of the random forest-derived Landsat-LiDAR maps also revealed that cashew plantations increased by 7. 5% and the bare ground increased by 70.
| Datasets We obtained information on density of occupied nest boxes per ha, nest box size, clutch size, laying date and ecological variables from all studies considered in this manuscript of two common species of secondary hole nesters, the great tit and the blue tit, across Europe and North Africa, as described in detail elsewhere  (Møller et al. , 2014a,b). Specifically, we obtained data on first clutches, or early clutches known to be initiated less than 30 days after the first egg was laid in a given year in a local study plot (cf. Nager & van Noordwijk, 1995). In total, we obtained information on 87 study plots with both great and blue tits breeding during the period 1957-2012  (Møller et al. , 2014a,b). We chose study plots where both great and blue tits had been recorded breeding at least once in order to ensure that all study plots contained suitable habitats, breeding sites and nest boxes for both species.
| Summary statistics The analyses of competition were based on a maximum of 978 plot by year estimates of laying date and clutch size varying due to differences in availability of data. We had data for a total of 87 plots where both species bred at least once. For great tits, mean laying date weighted by sample size was 23 April (SE = 0. 36, N = 929) and mean clutch size was 8. 61 eggs (SE = 0. 04, N = 970). For blue tits, mean laying date was 24 April (SE = 0. 41, N = 935) and mean clutch size was 9. 93 eggs (SE = 0. 06, N = 973).
g. Loisel et al. , 2006; Reynolds et al. , 2001; Stramska et al. , 2003) : 𝑏 𝑏𝑝 (𝜆) = 𝑏 𝑏𝑝 (𝜆 0 ). ( 𝜆 𝜆 0 ) -𝛾 (1) with γ=2. 5. This value is derived from in situ bbp measurements in the SPSG, at different wavelengths from the BIOSOPE dataset (during austral summer 2004). This γ value is in agreement with the study of  Loisel et al. (2006)   chlorophyll waters of subtropical gyres with high γ values (between 2 and 3) resulting from a dominance of small-sized particles. Finally, from bbp(555) estimates and using the POC vs. bbp(555) slope developed from the BIOSOPE dataset excluding upwelling data  (Stramski et al. , 2008) , bbp is converted into POC for FOpenO and FTWake. The dissolved oxygen concentration (O2) is derived from the Aanderaa optode measurements following the procedure described by  Thierry et al.
(2016). Based on the pre-deployment in-air measurements from FTWake, a factor of 1. 07 and no offset are applied to each O2 profile  (Bittig and Körtzinger, 2015). The SUNA sensor allows quantifying the nitrate concentration (NO3 -) from light absorption at ultraviolet wavelengths  (Johnson et al. , 2010 (Johnson et al. , , 2013;; Johnson and Coletti, 2002). As recommended by  Johnson et al. (2016) , NO3 -is calculated using the algorithm developed by  Sakamoto et al. (2009). All data used in this study are also pressure-corrected as suggested first by Pasqueron de  Fommervault et al. (2015)  and confirmed by laboratory measurements  (Johnson et al. , 2016 (Johnson et al. , , 2017a (Johnson et al. , , 2017b)). A post-deployment calibration is finally performed to correct data from instrumental drift.
HYCOM modelled ocean currents Ocean current dataset from daily archive of the 1/12° reanalysis of the Hybrid Coordinate Ocean Model (HYCOM, http://hycom. org; Chassignet et al. , 2009)  using the Navy Coupled Ocean Data Assimilation (NCODA) system is used to provide an overview of the currents in the study area and along the floats trajectories. The NCODA system  (Cummings, 2005; Cummings and Smedstad, 2014)  assimilates available satellite altimeter observations, satellite and in situ Sea Surface Temperature (SST) as well as available in situ vertical temperature and salinity profiles (from XBTs, Argo floats and moored buoys). The GLBu0. 08/expt_91. 1 experiment is hereafter used. Ocean currents (i. e. , speed as well as the zonal and meridian components) are extracted from the surface down to 300 m over the central SPSG, bounded by 170°W-140°W and 10°S-30°S, and from April 2015 to November 2016.
Altimetry-derived products To analyze fronts, transport barriers and horizontal stirring induced by surface currents, we investigate the Finite Size Lyapunov Exponents (FSLEs) that are passive Lagrangian diagnostics derived from ocean surface geostrophic currents (e. g. d  'Ovidio et al. , 2004; Mancho et al. , 2008). FSLEs are currently provided by AVISO+ (Archiving Validation and Interpretation of Satellite Oceanographic Data, www. aviso. altimetry. fr) with a spatial resolution of 1/25° and a temporal resolution of 4 days. These data are extracted over the same region and period as described in Section 2. 2 for the HYCOM dataset.
A more dedicated work based on lagoon modeling would help to explore further the nitrate supply up to 100 m depth since HYCOM does not take into account the specific lagoon dynamics and exchanges with the open ocean waters. Biogeosciences Discuss. , https://doi. org/10. 5194/bg-2017-541 Manuscript under review for journal Biogeosciences Discussion started: 10 January 2018 c Author(s) 2018. CC BY 4. 0 License. For the first time, the signature of an IME has been evidenced in a low nutrient low chlorophyll environment based on in situ observations collected from BGC-Argo floats. The BGC-Argo float in the Tahitian wake has allowed to describe a phenomenon that cannot be captured by satellites due to the high cloud coverage in the SPSG during the rainy season. The missing satellite data prevented the delineation of the IME geographical extension but thanks to in situ float measurements, the biological enhancement has been evidenced up to 20 km off Tahiti.
Exponent data used in this study. The 1/12 deg global HYCOM+NCODA Ocean Reanalysis was funded by the U. S. Navy and the Modeling and Simulation Coordination Office. Computer time was made available by the DoD High Performance Computing Modernization Program. The output is publicly available at http://hycom. org. Finally, data from the BIOSOPE transect of particulate backscattering coefficient at different wavelengths were taken from the BIOSOPE database available on the website: http://www. obs-vlfr. fr/proof/php/x_datalist. php?xxop=biosope&xxcamp=biosope; and access have been provided by C. Schmechtig.
Acknowledgements First, we would like to thank the  Government of French Polynesia  and the  French State  for providing funding support to the  THOT  project (Contrat de projets Etat-Pays, convention n°8690/MSR/ REC , and arrêté de subvention n°  HC/2860/DIE/BPT ), including the post doctorate fellowship of  R. Sauzède. This work was also supported by the  French national program LEFE/INSU  and the  French Ministry of the Overseas. FOpenO was provided by the remOcean project (funded by the  European Research Council , grant agreement  246777 ). We also thank the  French BGC-Argo program  (funded by  CNES-TOSCA, LEFE Cyber and LEFE-GMMC)  and the  Coriolis program  for providing standard Argo floats to be equipped with additional bio-optical and biogeochemical sensors. The BGC-Argo data were collected and made freely available by the  International Argo Program  and the national programs that contribute to it.
However, the slope of our ∆ 47 -temperature calibration line is indistinguishable from the brachiopod-only calibration of Came et al. 9  , made at 25 °C. ∆ 47 and δ 18 O offsets from apparent equilibrium. The difference between the measured and apparent equilibrium values are here referred to as offset values (Supplementary Data 2). Annual mean habitat temperatures (i. e. , brachiopod growth temperatures) were acquired from the World Ocean Atlas 2013  31. Annual mean seawater δ 18 O values representative of the sampling location and depth were taken from the Global Seawater Oxygen-18 Database  34. For thirteen out of eighteen specimens, directly measured seawater δ 18 O values were also available, giving actual seawater oxygen isotope compositions at the water depth where the brachiopods were collected  20  (Supplementary Table  1 ).
To remain consistent, we distinguish between the two datasets: one using only the seawater δ 18 O values acquired from the Global Seawater Oxygen-18 Database  34  and the other in which gridded δ  18  O values were replaced by the directly measured δ  18  O values where available. 1 ) were used for the calculations. For all plots: linear regression lines fitted to our data consider the errors. Corresponding two-tailed p-values are computed using a t-test. Error bars for the offset δ  18  O values indicate the mean deviation from oxygen isotope equilibrium calculated using the minimum and the maximum temperature estimates. Error bars for the offset ∆ 47 values indicate the 1σ S. E. of the replicate measurements. Apparent δ 18 O calcite equilibrium values were calculated using the 1000lnα calcite-water -temperature relationship of Kim and O'Neil  35  (see Supplementary Information) and that of Brand et al.
If this enzyme was present in brachiopods, it could reduce or eliminate the kinetic isotope effects caused by the slow hydration and hydroxylation reactions. However, carbonic anhydrase has not been identified in the calcifying fluid of modern brachiopods  57. Our data exhibits an offset ∆ 47 -δ  18  O slope of -0. 017(±0. 03) if the offset δ 18 O values are calculated using the seawater oxygen isotope compositions acquired from the Global Seawater Oxygen-18 Database 34 (Fig. 1b ). If the offset δ 18 O values are calculated using directly measured water δ  18  O values where possible, the offset ∆ 47 -δ  18  O slope becomes as steep as -0. 039(±0. 01) (Fig. 1c ). Both slopes are significant and stay consistent, irrespective of data processing, i. e. , [Gonfiantini] vs. [Brand] parameters, and the clumped isotope calibration we used to calculate the offset values (Supplementary Figs  2b,c  and 3 ).
The observed correlation slopes (-0. 017 to -0. 039, depending on the seawater δ 18 O dataset) between offset ∆ 47 and offset δ 18 O point to the importance of kinetic effects associated with diffusion and incomplete hydration and hydroxylation of CO 2(aq). The hydration and hydroxylation reactions occur superimposed onto the diffusion of CO 2(aq). Consequently, diffusion alone cannot be the sole kinetic mechanism responsible for the observed trend in our data. If heterogeneous oxygen isotope exchange between water and CO 2(aq) proceeds to equilibrium, it would erase the offsets from equilibrium ∆ 47 and δ 18 O generated during diffusion. Tang et al. 37  precipitated calcites at a pH < 9 and >10 and observed that ∆ 47 values increased by approximately 0. 016‰ for every 1‰ decrease in δ 18 O at high (>10) pH.
They suggested that a combined effect of diffusion and hydroxylation could be responsible for the observed slope. Interestingly, their slope is indistinguishable from the one we observe when we exclusively use the Global Seawater Oxygen-18 Database 34 to infer seawater δ 18 O. However, pH > 10 would be inconsistent with the internal pH range of modern brachiopods, which is likely to be between 7. 7 and 8. 2, calculated from δ 11 B values  41. Hydration is more prominent at low (<8. 4) pH while hydroxylation is more prominent at high (>8. 4) pH, assuming temperature and salinity values characteristic of modern seawater  49, 52  (Fig. 4 ). In the pH range characteristic for modern brachiopods, only 10-40‰ of the oxygen isotope exchange between water and CO 2(aq) should occur via the hydroxylation reaction, whereas 60-90% should proceed via the hydration reaction  52  (Fig.
4 ). Such a dominance of hydration over hydroxylation would result in an offset ∆ 47 -δ  18  O slope of -0. 034 to -0. 046, assuming estimated slopes of -0. 05 and -0. 01 to be characteristic of the hydration and hydroxylation reactions, respectively  12, 54. This range of slopes is in agreement with our result based on the dataset that combines gridded seawater δ 18 O data with directly measured values (Fig. 1c  and Supplementary Figs  2c  and 3b,d ). The δ 18 O values of the temperate modern brachiopod shells analysed in this study correlate well with corresponding δ 13 C values (R 2 = 0. 89, p-value < 0. 001; Fig. 5a ). Brand et al. 58  showed that parallel correlations are present between shell δ 18 O and δ 13 C among tropical (latitudes < 30°), temperate (latitudes 30°-60°) and polar (latitudes > 60°) brachiopods, respectively.
Stable isotope analyses. Clumped isotope analyses were made using a fully automated gas extraction and purification line connected to a ThermoFisher MAT 253 gas-source isotope-ratio mass spectrometer at the Goethe University, Frankfurt, Germany. Homogenised carbonate powder was reacted at 90 °C with >105% phosphoric acid. In general, six replicate analyses were made every day including one carbonate standard, one equilibrated gas (1000 °C or 25 °C) and four sample replicates. Background correction was performed for the sample and the reference gas separately, as described in Fiebig et al. 71  (Supplementary Fig. 5 ). Background-corrected equilibrated gas data displays slopes that are within errors indistinguishable from zero (Supplementary Data 1).
Acknowledgements We thank  S. Hofmann  and  C. Schreiber  ( J. W. Goethe-Universität ) for their technical assistance during the clumped isotope analyses,  D. Henkel  (GEOMAR) and  L. Angiolini  ( University of Milan ) for providing the P. atlantica and N. nigricans specimens and  R. Sheward  for language editing. This paper benefited from the constructive suggestions of  Kozue Nishida  and two anonymous reviewers. This project was funded by the  European Union 's  Horizon 2020 research and innovation program  under the  Marie Skłodowska-Curie  grant agreement No. 643084  ( BASE-LiNE Earth ).
Funding: This work is part of the research project  CGL2013-42643-P  funded by the  Spanish Ministry of Science, Innovation and Universities (former Ministry of Economy and Competitiveness). The grant supporting  C. Blanco-Moreno  was funded by the  Universidad Autónoma de Madrid. Acknowledgments: This work, which is part of the research projects CGL2013-42643-P was funded by the  Spanish Ministry of Science, Innovation and Universities (former Ministry of Economy and Competitiveness ). The  FPI-UAM  research grant supporting  C. Blanco-Moreno  was funded by the  Universidad Autónoma de Madrid. SEM observation was conducted at  SIdI UAM (Madrid)  and we thank  Esperanza Salvador ,  Isidoro Poveda  and  Enrique Rodríguez Cañas  for the help. We also thank  Antonio Romero  for the help using the rotary microtome.
This work is a review of Boris Choubert's paper (1935), which was published in French under the rather devalorizing title: "Research on the Genesis of Palaeozoic and Precambrian Belts. " Despite its innovative content, this article had no impact either at the time of its publication or even later. It begins with the construction of a remarkable fit of the circum-Atlantic continents. This was based on the À1. 000 meters isobath instead of the shoreline. Thirty years before  Bullard et al. (1965) , it demonstrated in an indisputable way the reality of the continents motion on the surface of the Earth. Therefore, Choubert designated Wegener's "continental drift" as the main cause of tectonics. Even going beyond Wegener's theory, he argued that this mechanism was efficient well before the formation of the Triassic Pangaea, during the whole Palaeozoic to result in the building of the Caledonian and Hercynian mountains.
Acknowledgements. This text was drawn up on the impulse of  Xavier Le Pichon  with  Hank Frankel 's encouragement. It was reviewed by  Philippe Huchon  and  Michel Faure  who were both relevant in their comments and benevolent in their conclusions; two other anonymous reviewers showed great goodwill. On behalf of the  French Geological Society ,  Laurent Jolivet  supported our initial project right away, while Solange Chaimbault was doing everything necessary to get the copyright of Choubert's initial paper. Elisabeth, Georges and  Pierre Choubert , as well as Alexandre,  Marion  and  Michel Schuberth  gave permission to the  French Geological Society  to reproduce text and figures from the article of their uncle Boris. Finally, thanks to  Félix Nolleau , the text presented above is written in a language much more polished and idiomatic than that of the initial manuscript.
The Evaluation Procedure The evaluation is carried out on four datasets with different 3D scene types, cameras and acquisition geometries. To obtain 3D accuracy measures, several Ground Control Points (GCPs) were measured in each scene. Each dataset is processed with two methods: the classical processing with SIFT tie-points (implementation of  [38] ) (Classical) and the SIROP method, which only uses its own-detected points. In any case, grayscale images are used to extract tie-points. The difference between the two processing methods is in the employed tie-points. In both scenarios the camera parameters are estimated in a self-calibration BBA (i. e. , the Fraser camera model  [39] ). The BBA computation is first carried out in a relative coordinate system, and further transferred to the coordinate system of the GCPs with the 7-parameter transformation estimated from all GCPs.
Three case studies are summarized in Table  1. XYZ = [1, 1, 2] cm 10 GPS RTK σ XYZ = [1, 1, 2] cm Each case study was processed according to the workflow presented in Figure  1. Due to repetitivity of the obtained results, only one detailed outcome analysis is presented-the terrestrial Hallway dataset in Section 3. 2. As for the UAV datasets (Viabon1, Corridor), a compiled presentation of the obtained results is given in Section 3. 3. The evaluation is carried out by looking at the following accuracy measures: • euclidean distance between GCPs resulting from image triangulation and their true values (d).
UAV Datasets The aim of this section is to asses the performance of SIROP in an aerial acquisition. Two UAV-acquisitions were processed: a block acquisitions (Viabon1-see Figure  26 ), and a corridor acquisition (Corridor). As detailed in Table  2 , SIROP outruns the Classical method in all the tested scenarios. The accuracy gain is observed particularly along the Z component, i. e. , along the coordinate with the highest estimation uncertainty due to the imaging configuration. Global increase in tie-points manifold is also observed. The Corridor dataset uncovers another beneficial aspect of SIROP, i. e. , the capability of suppressing the "dome" effect. It has been stated by many researchers  [8, 41, 42]  that under certain imaging configurations the self-calibrating BBA is suboptimal. The arising correlations between the camera internal parameters and the exterior orientations lead to incorrect modelling of both.
83, 1. 46 for the respective datasets. The tie-points manifold was increased in all but the Hallway dataset where far points were eliminated contributing to a slightly lower points' redundancy. To alleviate the issue and the potential camera's rotational drift, the low-resolution tie-points from the Classical method could be integrated with the SIROP tie-points (see Figure  30 ). Inspection of the UAV datsets revealed that SIROP tie-points contribute to a better estimation of the camera internal parameters and thus are capable of eliminating the systematic "dome" effect. Stability of the internal camera parameters calculated with SIROP has been also verified (see Figure  29 ). The processing time of SIROP is also evaluated by the Corridor dataset (see Figure  27  and Table  2 ) containing 77 panchromatic 20-megapixel images.
The classical framework at full-resolution, from the tie-points extraction to 3D mesh generator requires 234 minutes. SIROP is then applied using the 3D mesh and image orientation derived from the classical round. SIROP time consuming essentially depends on the number of images in dataset and the number of triangles in the 3D mesh. In this test, the 3D mesh contains 18021 3D triangles and SIROP processing takes 18 minutes. Overall, the method proved its efficiency and could be adopted as a post-processing step for fine metrology applications. Furthermore, SIROP could be used to accelerate the classical processing by using a very low resolution scene geometry calculated with a SIFT-like method at its input.
, 2014). In this study, we introduce recent developments in the field of climate information related to meteorological and natural snow conditions, applied to the French mountain areas. The approach draws on the use of the ADAMONT statistical adjustment method  (Verfaillie et al. , 2017)  applied to multiple historical  and future (2006-2100) EURO-CORDEX regional climate model runs spanning all relevant RCPs (RCP2. 6, RCP4. 5 and RCP 8. 5). The 13 GCM-RCM EURO-CORDEX pairs available in April 2017 (and for which the geopotential data for the corresponding CMIP5 GCMs were available) were used. These are expected to span the overall uncertainty resulting from GCM errors, RCM errors and climate internal variability. We used one of the longest meteorological reanalyses available in the French mountain regions -the SAFRAN reanalysis  (Durand et al.