dataesr/scientific-paragraphs-categorization huggingface dataset:
Acknowledgements We thank  Dr. Klaas Metselaar  ( Wageningen University ) for his support and collaboration in developing the methodological setup of this study. We thank the  Brazilian National Water Agency (ANA) , the  Research Institute of Meteorology and Water Resources (FUNCEME) , the  Water Company of the State of Ceará (COGERH)  and the  Brazilian Geological Service (CPRM)  for stream ow, meteorological, reservoir and groundwater data, respectively. Ethical Approval Not applicable.
Evolution of Ozone Columns and Comparison With Observations All CMIP6 models used in this study have been evaluated by  Keeble et al. (2021)  and  Morgenstern et al. (2020)  on stratospheric ozone, and by  Griffiths et al. (2021)  on tropospheric ozone using various observational datasets. Therefore, we do not carry out extensive model evaluations that have already been presented in those studies. As the purpose of this study is to attribute the ozone change to individual forcings, we focus on comparing modeled and observed ozone changes. Ozone observation data are obtained from the World Ozone and UV Data Center's ground-based climatology  (Fioletov et al. , 2002a). Colored lines are TCO deviations of individual model smoothed using a 5-year boxcar filter. Four models (CESM2-WACCM, MRI-ESM2-0, UKESM1-0-LL, and GFDL-ESM4) are included in the MMM.
The tropospheric ozone distribution and burdens in CESM2-WACCM, GFDL-ESM4, MRI-ESM2-0, and UKESM1-0-LL have been evaluated by  Griffiths et al. (2021)  using several observational datasets, including the Trajectory-mapped Ozonesonde data set (G. Liu et al. , 2013a; J. Liu et al. , 2013; Tarasick et al. , 2019)  and several satellite products, one of which is the Ozone Monitoring Instrument/Microwave Limb Sounder (OMI/MLS) product, the residual of the OMI total ozone column and the MLS stratospheric ozone column  (Ziemke et al. , 2006a). Griffiths et al. (2021)  find that the models and observations agree well on the increasing tropospheric ozone burden from 1997 to 2014, namely 0. 82 ± 0. 13 Tg yr -1 in the CMIP6 ensemble mean, 0. 70 ± 0. 15 Tg yr -1 in TOST, and 0. 83 ± 0. 85 Tg yr -1 in the satellite ensemble.
The ozone burden from the CMIP6 model ensemble is also comparable to that derived by  Gaudel et al. (2018). The comparisons between the tropospheric ozone columns from the four CMIP6 models against the TOST (1998-2012) and the OMI/MLS (2005-2014) datasets are shown in Figure  S7  of Supporting Information S1. The MMM contributions of the stratospheric and the tropospheric columns to the TCO changes in the histSST simulations are shown in Figure  10  over the whole simulation period (1850-2014) (The equivalent Figure  S9  in Supporting Information S1 showing column ozone changes in the coupled historical experiment indicates a minimal difference between the histSST and the historical simulations. ). Despite some large inter-model differences in TCO, the MMM TCO is in very good agreement with the observations in all regions and captures the observed interannual variability (Figure  9 ).
Data Availability Statement Data from all the CMIP6 CMIP and AerChemMIP simulations used in this study are available on the ESGF data archive (ESGF) https://esgf-node. llnl. gov/search/cmip6/. The data set citations for the models and the simulations are follows: CESM2-WACCM histSST (Danabasoglu, 2019a); CESM2-WACCM.
By integrating results of OROGEN with those of other recent collaborative projects in the Pyrenean domain (e. g. , PYRAMID, PYROPE, RGF-Pyrénées), this paper offers a synthesis of current knowledge and debate on the evolution of this immature orogen as recorded in the synorogenic basins and fold and thrust belts of both the upper European and lower Iberian plates. Expanding insight on the role of salt tectonics at local to regional scales is summarised and discussed. Uncertainties involved in data compilation across a whole orogen using different datasets are discussed, for example for deriving shortening values and distribution.
, 2002a; Schettino and Turco, 2009, 2011; Handy et al. , 2010). This small orogen has become one of the best-studied natural laboratories for collisional orogenic processes. Over the last 10 years, four major projects funded by French research agencies and industry have focused on various aspects of the Pyrenean Orogen: PYROPE (deep seismic tomography, funded by the French National Funding Agency, the ANR), PYRAMID (North Pyrenean foreland systems, funded by the ANR), the RGF-Pyrenees project (funded by the BRGM), and OROGEN (Orogenic Systems, funded by Total, CNRS and BRGM). These large collaborative projects, combined with other research programs in Spanish, French and international research institutions are driving an exceptional outpouring of new research on the Pyrenean orogen. As well as contributing to the ever-improving standard geological databases, these research efforts are building outstanding new datasets such as for passive seismic tomographic imagery of the orogen's deep structure and physical properties (e.
g. ,  Chevrot et al. , 2022)  and thermochronology datasets using a variety of isotopic systems (e. g. ,  Bosch et al. , 2016; Labaume et al. , 2016 , Labaume et al. , 2016; Vacherat et al. , 2016 Vacherat et al. , , 2017;; Bernard et al. , 2019; Odlum et al. , 2019; Ternois et al. , 2019a, b; Fillon et al. , 2020; Milesi et al. , 2020; Waldner et al. , 2021) , that provide insight into crustal thermal evolution and deformation during orogenesis. Thermomechanical modelling also offers an increasingly powerful and effective tool to investigate complex geodynamic systems and processes and their controlling parameters (e. g. ,  Beaumont et al. , 2000; Sinclair et al. , 2005; Mouthereau et al. , 2014; Erdös et al. , 2014a, b; Curry et al. , 2019; Grool et al. , 2019; Jourdon et al. , 2019 Jourdon et al.
They reveal along-strike variations in major lithospheric boundaries due, in part, to inherited rift segmentation but also to lateral variations in orogenic processes and amount of plate convergence. Prevalent models of crustal thickening by southward stacking of upper crustal imbricates with subduction of Iberian lower crust give relatively high estimates of total shortening along the ECORS-Central profile  (120-165 km; Fig. 4a; Beaumont et al. , 2000; Muñoz, 1992 Muñoz, , 2002 Muñoz, , 2019)). Alternative models for this section propose full crustal imbrication giving lower shortening estimates (92-100 km;  Roure et al. , 1989; Mouthereau et al. , 2014; Cochelin et al. , 2018; Bellahsen et al. , 2019; Waldner et al. , 2021). This illustrates how uncertainties in structural interpretation and in the datasets used can strongly impact cross-sectional models (see  Bond, 2015; Randle et al.
High resolution dating and correlation of such key non-marine, fossil-poor successions is a major challenge. In the Orogen project, high resolution chemostratigraphy (d 13 C org ) using terrestrial organic matter was combined with magnetostratigraphic and sparse biostratigraphic data to achieve a high resolution chronostratigraphy in this continental succession both in the NE Pyrenees  (Maufrangeas et al. , 2020)  and in the Tremp Basin, SE Pyrenees  (Vinciguerra, 2020 : Vinciguerra et al. , 2022). Thermal or climatic events in the global isotopic record are identified by correlation with the d 13 C record of marine reference successions. As well as being a powerful correlation tool, such high-resolution chemostratigraphy allows us to better constrain how much time is missing in the stratigraphic record and to understand why such gaps are created.
Dating the onset of Pyrenean shortening Constraining the timing of onset of convergence in an orogen using different datasets can give contradictory results. However, along and across the Pyrenean domain estimates for the onset of convergence-related deformation are remarkably consistent whether derived from tectonostratigraphic field observations, foreland basin subsidence histories described here and elsewhere (Figs. 2, 5b and 5c; e. g. ,  Teixell et al. , 2018; Muñoz, 2019)  or low temperature thermochronology (e. g. ,  Mouthereau et al. , 2014; Ternois et al. , 2019a, b). Bracketed between the late Santonian and early Campanian (84-83 Ma) these dates correspond well with the onset of Africa-Europe convergence (Fig. 2 ;  Olivet, 1996a, b; Srivastava et al. , 2000; Vissers and Meijer, 2012a, b; Macchiavelli et al.
Prowedge geometry and dynamics The prowedge consists of the Axial Zone and south Pyrenean thrust belt, which links westward across the Pamplona transfer zone with the Basque-Cantabrian belt (Fig. 3 ). The southern Pyrenees are probably one of the bestknown thrust belts in the world due to extensive research facilitated by outstanding exposures, accessibility, an excellent open access geological database and deep geophysical imagery. Thrust sheets were emplaced southward onto the Iberian plate from Late Cretaceous onward but principally during early Eocene-early Miocene main collision. Eocene-Miocene growth of the prowedge and its foreland basin is principally controlled by plate kinematics, critical wedge dynamics and its interactions with surface processes and the distribution and thickness of Upper Triassic and other evaporitic levels.
Thermal record of Early Convergence In convergent settings, syn-orogenic cooling of crustal rocks, measured by low temperature thermochronology methods, is generally assumed to record rock exhumation by surface uplift and erosion in the evolving orogenic wedge  (Reiners et al. , 2005; Reiners and Brandon, 2006; Carrapa, 2010). Extensive Pyrenean bedrock and detrital low temperature thermochronology datasets essentially support this model recording diachronous exhumation along and across the North Pyrenean massifs and Axial Zone principally from Eocene (50 Ma) to Miocene  (Yelland, 1990 (Yelland, , 1991;; Morris et al. , 1998; Fitzgerald et al. , 1999; Sinclair et al. , 2005; Jolivet et al. , 2007; Filleaudeau et al. , 2011; Whitchurch et al. , 2011; Fillon and van der Beek, 2012; Mouthereau et al.
4  and 7 ) of the Internal Metamorphic Zone  (Chelalou et al. , 2015; Clerc et al. , 2016; Ternois et al. , 2019a, b; Ducoux et al. , 2021a). A fragment of peridotite is also preserved in the IMZ Boucheville syncline, attesting to associated mantle exhumation (Fig. 7g ). The basement massif itself did not, however, reach temperatures of more than 350 °C during early Cretaceous rifting, except along discrete fault zones  (Ternois et al. , 2019a, b). The Agly-Salvezines block records extreme crustal thinning dated as early Cretaceous  (Odlum et al. , 2019). Combining geological studies with inverse and forward modelling of single-grain AHe ages and a large ZHe dataset from this massif,  Ternois et al. (2019a, b)  build a robust model of syn-orogenic tectonic and thermal evolution, identifying two cooling episodes, one in Late Campanian-Maastrichtian and the other in Ypresian-Bartonian, as well as an earlier syn-rift cooling signal.
, 2019). Substantial erosion of Miocene sediments also limits the resolution of late stratigraphic signals across southern deformation fronts. Finally, the drastic change in base level that occurred around 10 Ma generated its own strong erosional isostatic rebound. Datasets tracking vertical motions (e. g. , low temperature thermochronology data) that have detected this strong post-convergence motion lack, as yet, sufficient resolution to distinguish any preceding weaker signal, for example, that of a post-orogenic rebound that would have started some 10 Myrs before. If we exclude the easternmost Pyrenees where Gulf of Lion extension dominated late to post-convergence dynamics, there is now general agreement that, the change from an endorheic to an exorheic base-level in the Ebro Basin exerted the principal control on late to post-convergence vertical motions and topographic development across the southern Pyrenean foreland system rather than the end of plate convergence or other factors such as climate  (Fillon and van der Beek, 2012; Fillon et al.
Conclusions and future challenges As a small low convergence collisional orogen the Pyrenees preserves an excellent record of the progressive establishment of continental subduction without being preceded by oceanic subduction. The orogen provides a record of early rift inversion often destroyed or overprinted in more mature orogens. The record also demonstrates that orogen behavior changed markedly, during two critical transitions, early convergence to main collision and main collision to post-convergence, reflecting changes in lithospheric processes and in the role of different tectonic drivers. Studies in the Orogen, RGF Pyrenees and ANR-PYRAMID projects have focused principally on the northern Pyrenees, where the inverted rift system is preserved. These projects have produced considerable new knowledge and data on a wide range of issues including the two critical transitions and the early convergence period.
Outstanding new datasets have been provided by passive seismic tomographiy campaigns (ANR-PYROPE and Orogen projects;  Chevrot et al. , 2022 and references therein)  and new low temperature thermochronology analytical techniques and isotopic dating techniques (e. g. ,  Airaghi et al. , 2019; Ternois et al. , 2019a Ternois et al. , , b, 2021a, b;, b; Fillon et al. , 2020; Léger et al. , 2021). Principal findings are summarized below: -A preexisting rift is essential for the development of a doubly vergent orogen. Thermal, rheological and structural rift inheritance impacts all aspects of orogen evolution, particularly during early orogenesis. -During early convergence, plate forces were distributed across the near and far field causing inversion of rift structures and depocentres across Europe as stress was transmitted across a sufficiently strong plate boundary.
g. , calcite dating of faults,  Hoareau et al. , 2021; Parizot et al. , 2021)  also have the potential to provide high resolution tracking of rock trajectories and thermal evolution of the orogen. As shown by recent studies the application of new concepts and ideas developed in the domain of salt tectonics are providing significant new data and challenging established models on basin and orogen dynamics in the Pyrenees. Future challenges to improve investigations into orogen structure, rheology and processes include the need to better integrate large geophysical datasets (e. g. , passive seismic tomography) and uncertainty analysis of structural interpretations, and to improve statistical analysis of large and complex analytical datasets (e. g. , low temperature thermochronology).
Acknowledgements. This paper is a contribution to the  Orogen  project funded by  Total , the  BRGM  and the  CNRS. It is also a contribution to the  ANR PYRAMID  and  RGF Pyrénées  projects. While all authors have contributed to this work, the opinions are biased toward those of the first author. The authors salute and thank the whole  Orogen Community  and the innumerable colleagues and experts of the  Pyrenean geoscience community. This work has grown from and greatly benefited from discussions with them all. We thank reviewers  P. Labaume  and  A. Casas-Sainz  and editor  A. Teixell  for their constructive reviews that greatly improved the manuscript.
2) Does pellet detectability differ between types of sampling units and between tundra vegetation types? We assessed if the detectability of pellets differs when using different types of sampling units (linear transects or smaller sampling plots). We used data from three study areas (Erkuta and Sabetta on Yamal Peninsula, and Isfjorden in Svalbard) where fecal pellets were counted both along 30-m linear transects (30, 30 and 23 transects respectively) and in small plots (50x50 cm) located every 2 m along the transects. For each study area, we compared the density of pellets (pellets/m 2 ) estimated on the transects and in the smaller plots for different herbivore taxa. Deviations from a 1:1 correspondence between the two methods are interpreted as over-or under-estimation by one of the methods.
3) How does sampling effort affect pellet count estimates and how should sampling effort be distributed across a study area? To evaluate how transect length at the site level and transect length and the number of transects at the study area level influenced the precision of pellet density estimates we used simulations based on observed data. Site levelwe assessed the influence of transect length on the precision of pellet density estimates within sites (homogeneous habitat) simulating small habitat patches (250 x 250 m) with homogeneous pellet distribution. We used the observed data for one of the ITEX sites in Endalen located in a moss tundra habitat on a concave landform. We selected this site because it had the largest contrast in mean pellet density between the three herbivore taxa (reindeer, geese and ptarmigan).
4) Can the protocols detect the occurrence of all herbivores and capture differences in herbivore communities within sites and across study areas? Site level -to assess the ability of the protocol to detect all herbivore taxa present within a relatively homogeneous area, as in the case of the ITEX sites, we used the data from Endalen comprising five ITEX sites located on five distinct landscape units: a snowbed community dominated by bryophytes (Sanionia uncinata, Tomentypnum nitens) and Bistorta vivipara, a moist Cassiope tetragona heath, a moist moss tundra dominated by bryophytes (Sanionia uncinata) occurring in two contrasting parts of the landscape (a concave and a convex land form), and an exposed Dryas octopetala heath. For each site we built species accumulation curves using the specaccum function in the vegan package in R  (Oksanen et al.
2019 ). Since only one transect was conducted at each site, we randomized the order of segments within each transect to assess how many species of herbivores were detected with increasing transect length (100 permutations). We also plotted the observed species accumulation curve along the transects (i. e. same order of meter segments) in each habitat because we found some spatial autocorrelation between meter-segments (Figure  S1 ). Study area -to assess how sampling effort (i. e. transect length and the number of transects) affects our ability to detect herbivore taxa over heterogeneous study areas, we used data from the three study areas (Erkuta, Sabetta and Isfjorden). For each study area, we built species accumulation curves estimated from 100 random permutations of transects and for transect lengths between 5 and 30 m.
Here we measured herbivory more coarsely by using a modified point-intercept method that estimates the percentage of sampling points affected by herbivory. Nevertheless, our results are within the same order of magnitude as other studies measuring invertebrate herbivory in the tundra  (Barrio et al. 2017; Rheubottom et al. 2019). Additionally, the method described here bears some similarity to the widely used transparent grid method  (Coley 1983 , Pearse and Hipp 2009 , Henderson and Southwood 2016) , which has been shown to accurately measure insect herbivory on plants  (Getman-Pickering et al. 2020). The current protocol therefore provides a rather fast way of assessing the relative intensity of invertebrate herbivory that can be implemented at different sites. In addition, the pointintercept method is widely used in tundra vegetation studies, so information on plant damage can be combined with species composition data to obtain species specific damage and facilitate estimates of community-wide herbivory  (Zvereva et al.
TABLES AND FIGURES1 Table  1. List of study areas and sites included in the plot-level assessment. A study area can include several International Tundra Experiment (ITEX) sites. Sites including ITEX experimental manipulations are indicated with asterisks. At some ITEX sites, Open Top Chambers (OTCs) and control plots are located adjacent to each other (i. e. paired), while at others, OTCs and controls are randomly distributed across the site. Study areas are indicated by triangles in Figure  2. Random locations for 2 m wide transects between 10 and 150 m long were simulated (transect area between 20 and 300 m 2 ) in a homogeneous habitat; for each transect length, the simulated sampling was carried out 500 times. Data is based on pellet counts at an International Tundra Experiment (ITEX) site in Endalen, Svalbard (concave moss tundra) for the most abundant herbivore taxa (reindeer, goose and ptarmigan).
Data is based on pellet counts at an International Tundra Experiment (ITEX) site in Endalen, Svalbard (concave moss tundra) for the most abundant herbivore taxa (reindeer, goose and ptarmigan). Note the different y-axis scales by species. Transect area is presented here for comparability to Figure  9. © The Author(s) or their Institution(s) Arctic Science Downloaded from cdnsciencepub. com by 185. 37. 110. 40 on 04/18/21 For personal use only. This Just-IN manuscript is the accepted manuscript prior to copy editing and page composition. It may differ from the final official version of record.
This site description should be completed once for each ITEX site. Background data on the potential occurrence and densities of herbivores and their distribution will help in defining overall herbivore activity in the area. This information will also help in defining the methods for herbivory assessment at the site-and plot-level (sections 2 and 3). Ideally levels 2 and 3 will be conducted once in the season every year if possible, but 'snapshot data' from different years will also be very useful.
It is thus very important to note in your field data collection if the visit corresponds to a first survey of a transect or not. When species identification is not possible from the pellets, pellets will be assigned broadly to groups of herbivores (e. g. , large mammals, small mammals, birds); whenever possible, take a picture of the 'unidentified' pellets. For large mammals (caribou/reindeer, moose, sheep, muskox), some medium-sized mammals (marmots;  Karels et al. 2004 )) and birds (swans, geese, ptarmigan) walk the transect down slowly (Figure  A3 ), recording the presence of pellets within every transect meter. If you are applying 30 m transects, pellets can be recorded by one observer within a 1-m band (0. 5 m to each side of the transect line). Alternatively, you could use 15 m transects with a 2-m band (1 m to each side of the transect; using a 2m stick as a reference with two people walking on each side of the transect line is helpful).
Figure6. Effect of transect area (m 2 ) on the mean (95% Confidence Interval, shaded areas) estimated number of pellets per m 2. Random locations for 2 m wide transects between 10 and 150 m long were simulated (transect area between 20 and 300 m 2 ) in a homogeneous habitat; for each transect length, the simulated sampling was carried out 500 times. Data is based on pellet counts at an International Tundra Experiment (ITEX) site in Endalen, Svalbard (concave moss tundra) for the most abundant herbivore taxa (reindeer, goose and ptarmigan). Note the different y-axis scales by species. Transect area is presented here for comparability to Figure9.
Identify the focal vegetation or landscape strata. If habitat preferences of herbivores in the study area are not known, data from the literature or expert knowledge from other areas can be used. Alternatively, an initial survey could be performed to assess habitat preferences. In this aim, pellet © The Author(s) or their Institution(s) Arctic Science Downloaded from cdnsciencepub. com by 185. 37. 110. 40 on 04/18/21 For personal use only. This Just-IN manuscript is the accepted manuscript prior to copy editing and page composition. It may differ from the final official version of record. © The Author(s) or their Institution(s) Arctic Science Downloaded from cdnsciencepub. com by 185. 37. 110. 40 on 04/18/21 For personal use only. This Just-IN manuscript is the accepted manuscript prior to copy editing and page composition.