dataesr/scientific-paragraphs-categorization huggingface dataset:
13039/ 501100011033/  and by  FEDER (UE) , the project  Tech2Coast  ( TED2021-130949B-I00 ) funded by  MCIN/AEI/ 10. 13039/501100011033  and by  EU "NextGenerationEU/PRTR " and the project  EuroSea  funded by he  European Union 's  Horizon 2020 Research and Innovation Programme  under grant agreement No. 862626. This study is a contribution to the  IM22MPDH  project, funded by the  EMFF (European Maritime Fishing Funds)  Data collection framework, the " Departamento de Desarrollo Económico y Competitividad " of the  Basque Government  and the " Secretaría General de Pesca " of the  Spanish Government  providing the oceanographic vessels  Emma Bardán. Ivan Manso-Narvarte  was supported by a PhD fellowship from the  "Departamento de Medio Ambiente, Ordenación del Territorio, Agricultura y Pesca" of the Basque Government.
Furthermore, the demonstration experiment allowed us to focus SD measurements on different marine ecosystems using multiple seasons, which made it possible to assess the quality of measurements across a wide range of values. The experiment additionally evaluated the ability of such ASVs to provide high-quality data for the scientific community. The objective of the present work is to evaluate and correct the data collected by the SDs and to provide a homogenised and comparable dataset that is useful to study processes in the Atlantic Ocean and Mediterranean Sea.
Saildrones (SD) The SDs, provided by Saildrone Inc. were equipped with a number of autonomous sensors (CTD, dissolved oxygen, fluorescence, pH, pCO2 and meteorological sensors) and here we focus primarily on the sensors that regularly measured temperature, salinity, dissolved oxygen, and pCO2. This selection is based on available options for correcting the SD datasets: some of the sensors (e. g. , fluorescence) were affected by biofouling to such a degree that it could not be accounted for and others worked only for a short period of time (e. g. , Durafet Honeywell pH sensor). One of the SDs (SD 1030) was equipped with an ASVCO2 system developed by PMEL (NOAA's Pacific Marine Environmental Laboratory). The ASVCO2 system is a compressed version of the more voluminous system https://doi. org/10.
A huge amount of data covering a large area from the eastern North Atlantic to the northern central Mediterranean has been produced, which required quality control and assurance to a varying degree, primarily depending on how sensitive the sensors were to biofouling. Due to the COVID-19 pandemic restrictions, there was a lack of validation samples collected from cruise transects, and this has enforced a new way of thinking regarding drift correction. The SBE salinity sensors at the SDs have been corrected, when necessary, using model products and the method was validated by comparing the data corrected with available in situ measurements. The Aanderaa dissolved oxygen sensors at the SDs were corrected using a new method that uses the in air oxygen measurements to correct the trend. The corrected SD datasets fit well with data from fixed stations and gliders, which means that the correction methods used are valid.
The output is data sets which are available for process interpretations in future research. One limitation of the correction methods has been the limited amount of validation points like Argo floats, fixed stations, cruises etc. This has been solved by taking model products into consideration. Notwithstanding the limitations of the method for correcting the data the use of the model ensures remarkable consistency, guaranteeing consistent correction in both space and time. Other SD sensors were affected by biofouling to such a degree that the datasets were unable to correct given the limited samples for validation, like e. g. the optical sensors for fluorescence measurements. Some recommendations connected to this are put forward in the next section.
Regarding correction of dissolved oxygen, it is advised to facilitate an in air calibration like the one used for Argo floats. This would require some reorganisation of the sensors, however, it will be easier to correct for drift of the oxygen sensor. It is also advised to look into the location of the SD sensors. For instance, the RBR sensor at the SD 1053 measured significantly lower dissolved oxygen compared to the SBE. One possible explanation for this could be that the RBR sensor was mounted inside the ship keel where dead water could accelerate the sensor fouling. The sensor mounting must ensure that the SD sensors are mounted correctly to sample open water. The ATL2MED demonstration experiment suffered by lack of discrete samples for validation. Thus, future experiments should be organised in such a way that discrete samples for salinity, oxygen, carbon, and chlorophylla are collected at a reasonable frequency, which will ease the validation of the SD dataset quality tremendously.
Acknowledgement. The ATL2MED experiment has received generous funding from the  US company PEAK 6 Invest  and invaluable support regarding coordination, operation, and data deliverance from  Saildrone Inc. Furthermore , funding has been provided by  GEOMAR Helmholtz Centre for Ocean Research (GEOMAR) ,  Integrated Carbon Observation System -Ocean Thematic Centre (ICOS-OTC) , the  French National Centre for Scientific Research (CNRS) ,  Oceanography Laboratory of Villefranche (LOV) , the  Oceanic Platform of the Canary Islands (PLOCAN) ,  Ocean Science Centre Mindelo (OSCM) , the  Hydrographic Institute of Portugal (IH) ,  Balearic Islands Coastal Observing and Forecasting System (SOCIB) ,  Italian National Institute of Oceanography and Applied Geophysics (OGS) ,  Helmholtz Zentrum Geesthacht (HZG) ,  Centre Scientifique de Monaco (CSM) ,  National Research Council-Institute of Marine Sciences (CNR-ISMAR) , and  National Research Council -Institute for the study of Anthropic   Impact and Sustainability in the Marine Environment  ( CNR-IAS).
Speleogenesis implications: regressive erosion of altered rock zones The unexpected result of diminished burial ages shown in Figure  3  came from the 4 Lazarc plateau caves that are distant of at least 2. 5km from any nearby river channel (Fig. 2 ). These caves have a clear classical tiered morphology that can be seen on the KARST3D database (KARST3D, 2019). Quartz rich sediments in Rocas are only located from -20m to -40m deep below the surface (555m -575m a. s. l. ) while the deepest part humanly accessible of the cave is at -130m (465m a. s. l. ) (Fig. 5 ). In Fonctionnaire, the sediments are in the lowest of the 3 levels, at -75m below the surface (520 m a. s. l. ). The Leicasse, which has 16km of mapped passages, alluvium is deposited in a ~1km long passage at more that -140m below the surface (440 m a.
Acknowledgments We thank  C. Mifsud ,  K. Stevens  and  S. Kotevski  for their assistance during the sample processing. We thank  K. Wilcken  for assistance in some of the earlier AMS measurements. We also thanks  Y. Guessard ,  L. Bruxelles ,  M. Roux  and  L. Leterme  for the identification of cave infilling or their help during sampling.
Long-term observatories are also dealt with in this special issue:  Chabaux et al. [2023]  use the Strengbach Critical zone observatory (France), integrating petrological and hydrogeological information from boreholes and piezometers, to characterize water circulation channels at the catchment scale. Aquifer properties are addressed in several of the papers:  Dumont et al. [2023]  present work on the Andesitic volcanic hydrosystems of Indonesia, using electrical resistivity tomography to characterize the aquifer and further parameterize the hydrological model structure. Malard et al. [2023]  present a flow animation module (FAM) designed to increase the understanding of dynamic hydrogeological processes within a web-based modelling tool called Visual KARSYS. Jost et al. [2023]  present their investigations relative to the link between gravel pit lakes and aquifers: they detail a gravel pit lake module developed for the CaWaQS modelling platform, which they test against the LAK package of Modflow.
Acknowledgment RB is partially supported by the  GNAMPA group of INdAM  and the  Royal Society International Exchange  Grant. This work has received funding from the  PRIN Project (MUR, Italy ) n. 20204NT8W4  Nonlinear evolution PDEs, fluid dynamics and transport  equations: theoretical foundations  and applications. TP acknowledges  Istituto per le Applicazioni del Calcolo (IAC-CNR)  for hospitality and financial support. Some computations in Section 5. 1 have been realized, in the framework of plane waves, when RB was holding a postdoc position under the mentorship of  A. -L. Dalibard  and  L. Saint-Raymond : RB warmly thanks both of them for their support. Finally, we both thank  Thierry Dauxois  for several discussions concerning experiments related to this work.
Deep incised glacial valleys surrounded by high peaks form the modern topography of the Southern Patagonian Andes. Two Miocene plutonic complexes in the Andean retroarc, the cores of the Fitz Roy (49°S) and Torres del Paine (51°S) massifs, were emplaced at 16. 7±0. 3 Ma and 12. 5±0. 1 Ma, respectively. Subduction of ocean ridge segments initiated at 54°S, generating northward opening of an asthenospheric window with associated mantle upwelling and orogenic shortening since 16 Ma. Subsequently, the onset of major glaciations at 7 Ma caused drastic changes in the regional topographic evolution. To constrain the respective contributions of tectonic convergence, mantle upwelling and fluvio-glacial erosion to rock exhumation, we present inverse thermal modeling of a new dataset of zircon and apatite (U-Th)/He from the two massifs, complemented by apatite 4He/3He data for Torres del Paine.
, 2009 Guillaume et al. , , 2013;; Scalabrino et al. , 2010; Fosdick et al. , 2013; Stevens Goddard and Fosdick, 2019; Georgieva et al. , 2016 Georgieva et al. , , 2019)). Mantle upwelling during ocean ridge subduction is expected to have generated long-wavelength dynamic surface uplift and lateral tilting of the continent, following the northward motion of the CTJ  (Guillaume et al. , 2009; 2013). In this study, we present new low-temperature thermochronological datasets from two of the most emblematic massifs of the Southern Patagonia Andes: the Fitz Roy  (FzR, 49°S)  and Torres del Paine (TdP, 51°S) (Figs. 1 2 3 4 ). These two regions are located south of the CTJ, and thus may have recorded the earlier effects of northward ridge subduction and asthenospheric window opening besides those of late Cenozoic glaciation  (Thomson et al.
AHe and ZHe thermochronological data We present all analytical details, as well as full AHe and ZHe data in Tables  1 2 3. For illustration, we report in Figure  5  both single-crystal and average AHe and ZHe corrected ages with 1 standard deviation of the single-crystal ages (1σ error) in age-elevation diagrams. The FzR dataset (Fig. 5a ) reveals single-crystal ZHe ages ranging from 6. 1±0. 4 to 12. 9±0. 8 Ma, and single-crystal AHe ages ranging between 3. 1±0. 1 and 9. 7±0. 6 Ma. The lack of clear age-elevation relationship for the entire elevation profile potentially indicates fast rock exhumation during the ~3 to 13 Ma period. For the TdP massif, single-crystal AHe ages from the Central sector (Fig. 5b ) range from 3. 1±0. 1 to 13. 1±0. 3 Ma, and the metasedimentary samples have similar ages to the magmatic samples.
The highest sample (FZR3, Fig. 6a ) reached surface temperatures at early Pliocene time, while the lowest elevation sample (FZR13, Fig. 6b ) still experienced cooling at 5 °C/Myr with a slight increase up to 20 °C/Myr at since 1 Ma. For the TdP massif, inverse thermal modeling using QTQt provided variable information on the regional exhumation history from the different sectors. For the Central sector (Figs. 7 and S2), expected T-t paths from the dense AHe dataset (Fig. 5b ) first show apparent rapid but unconstrained cooling from the imposed magmatic temperature/age constraints to a temperature range of 70-130 °C at around 11. 5 Ma, which is the oldest thermochronological AHe age in the profile. We propose that this cooling signal has no real geological meaning since it reflects thermal adjustment after the shallow intrusion of the TdP Plutonic Complex (note that the Central sector includes also two metasedimentary samples, which we assume were re-heated by the same intrusion event).
TdP samples of the Central sector then slowly cooled until 6. 5 Ma, when they experienced an increase in cooling rate from <1 °C/Myr up to 90-120 °C/Myr. This fast exhumation phase was relatively short in time (during 0. 5 Myr), ending at ~6 Ma, when the highest elevation sample (04-JM-66, Fig. 7a ) reached almost surface temperatures. The lowest elevation sample (13-TP-26, Fig. 7b ) shows a quiescent period until 2 Ma (slow cooling at <1 °C/Myr) when it experienced an increase in cooling rate up to 30 °C/Myr. It is worth noting that the output thermal history is relatively well constrained over the late Miocene to Plio-Quaternary period because of the dense AHe dataset and well prescribed AHe age-elevation relationship (Fig. 5b ). For the North and West sectors of the TdP Massif (metasedimentary samples, Fig.
8 ), the AHe dataset is less dense and output model predictions are less constrained. For the West sector, the expected T-t paths (Fig. 8a, b ) are not well constrained until 12 Ma, after this time the relative probability for the cooling histories defines a slow cooling at 4 °C/Myr. At around 6. 5 Ma, cooling accelerated to 25-30 °C/Myr for a short period of 1-1. 5 Myr, bringing the high-elevation sample (Fig. 8a ) to near surface temperatures. After this time-interval, the lowelevation sample (Fig. 8b ) was cooled slowly to the surface (at ~2 °C/Myr), with a potential late-stage exhumation increase since 0. 5 Ma (with a cooling rate up to 80 °C/Myr). For the North sector, there is no output constraint on the thermal histories until 15 Ma (Fig. 8c, d ). The output thermal history reveals slow cooling between 15 and 5 Ma, with an estimated cooling rate <2 °C/Myr, followed by a short cooling episode between 5 and 4 Ma at 40-60 °C/Myr.
The low-elevation sample (Fig. 8c ) also recorded cooling after 4 Ma, but this phase is relatively unconstrained, although a potential acceleration in cooling rate may occur since 0. 5 Ma (from 20 up to 40 °C/Ma, Fig. 8d ). Potential cooling events before 15 Ma would not have been recorded by the AHe dataset in the TdP massif. All TdP sectors show a short episode of fast cooling between 6. 5 and 4 Ma, which is common between the magmatic and the metasedimentary samples, and a potential delay (or lower precision in timing) for this event north of the TdP massif (North sector). Finally, the final stage of cooling is revealed for all low-elevation samples (Figs. 7b  and 8b,d ), but the timing of onset for this episode appears spatially variable, being apparently earlier (at 2 Ma) for the Central sector compared to the West and North sectors (at 0.
Abstract Deep incised glacial valleys surrounded by high peaks form the modern topography of the Southern Patagonian Andes. Two Miocene plutonic complexes in the Andean retroarc, the cores of the Fitz Roy (49°S) and Torres del Paine (51°S) massifs, were emplaced at 16. 7±0. 3 Ma and 12. 5±0. 1 Ma, respectively. Subduction of ocean ridge segments initiated at 54°S, generating northward opening of an asthenospheric window with associated mantle upwelling and orogenic shortening since 16 Ma. Subsequently, the onset of major glaciations at 7 Ma caused drastic changes in the regional topographic evolution. To constrain the respective contributions of tectonic convergence, mantle upwelling and fluvio-glacial erosion to rock exhumation, we present inverse thermal modeling of a new dataset of zircon and apatite (U-Th)/He from the two massifs, complemented by apatite 4 He/ 3 He data for Torres del Paine.
1 )  (Cande and Leslie, 1986; Thomson et al. , 2001; Ramos, 2005; Haschke et al. , 2006; Lagabrielle et al. , 2010; Breitsprecher and Thorkelson, 2009; Guillaume et al. , 2009 Guillaume et al. , , 2013;; Scalabrino et al. , 2010; Fosdick et al. , 2013; Stevens Goddard and Fosdick, 2019; Georgieva et al. , 2016 Georgieva et al. , , 2019)). Mantle upwelling during ocean ridge subduction is expected to have generated long-wavelength dynamic surface uplift and lateral tilting of the continent, following the northward motion of the CTJ  (Guillaume et al. , 2009; 2013). In this study, we present new low-temperature thermochronological datasets from two of the most emblematic massifs of the Southern Patagonia Andes: the Fitz Roy (FzR, 49°S) and Torres del Paine (TdP, 51°S) (Figs. 1 2 3 4 ). These two regions are located south of the CTJ, and thus may have recorded the earlier effects of northward ridge subduction and asthenospheric window opening besides those of late Cenozoic glaciation  (Thomson et al.
The highest sample (FZR3, Fig. 6a ) reached surface temperatures at early Pliocene time, while the lowest elevation sample (FZR13, Fig. 6b ) still experienced cooling at 5 °C/Myr with a slight increase up to 20 °C/Myr at since 1 Ma. For the TdP massif, inverse thermal modeling using QTQt provided variable information on the regional exhumation history from the different sectors. For the Central sector (Figs. 7  and S2 ), expected T-t paths from the dense AHe dataset (Fig. 5b ) first show apparent rapid but unconstrained cooling from the imposed magmatic temperature/age constraints to a temperature range of 70-130 °C at around 11. 5 Ma, which is the oldest thermochronological AHe age in the profile. We propose that this cooling signal has no real geological meaning since it reflects thermal adjustment after the shallow intrusion of the TdP Plutonic Complex (note that the Central sector includes also two metasedimentary samples, which we assume were re-heated by the same intrusion event).
8 ), the AHe dataset is less dense and output model predictions are less constrained. For the West sector, the expected T-t paths (Fig. 8a, b ) are not well constrained until 12 Ma, after this time the relative probability for the cooling histories defines a slow cooling at 4 °C/Myr. At around 6. 5 Ma, cooling accelerated to 25-30 °C/Myr for a short period of 1-1. 5 Myr, bringing the high-elevation sample (Fig. 8a ) to near surface temperatures. After this time-interval, the lowelevation sample (Fig. 8b ) was cooled slowly to the surface (at ~2 °C/Myr), with a potential late-stage exhumation increase since 0. 5 Ma (with a cooling rate up to 80 °C/Myr). For the output thermal history reveals slow cooling between 15 and 5 Ma, with an estimated cooling rate <2 °C/Myr, followed by a short cooling episode between 5 and 4 Ma at 40-60 °C/Myr.
the Quaternary, highlighting erosional quiescence and possibly reflecting bedrock shielding by extensive icefields covering the Southern Patagonian Andes. A late-stage Quaternary episode of accelerated rock exhumation is recorded in our thermochronological datasets, and coincides with worldwide increased mountain erosion ascribed to intense glacial-interglacial cycles. This climatic transition generated a geomorphological shift from smooth landforms to deep incised glacial valleys, leaving the high elevations of the Torres del Paine and the Fitz Roy plutonic complexes standing far above nearby valley bottoms. 7. Acknowledgments This work has also been supported by the Italian Ministry of Education, MIUR (Project Dipartimenti di Eccellenza 2023-2027, TECLA, Department of Earth and Environmental Sciences, University of Milano-Bicocca).
The Université Grenoble Alpes, the French CNRS, the INSU SYSTER project, and the ECOS-SUD project A15U02 also supported this work. V. A. P. M. acknowledges the ERASMUS+ program for the mobility grant to visit the Université Grenoble Alpes, and the TRB team. P. G. V. acknowledges funding support from the Swiss National Science Foundation SNSF (Grant PP00P2_170559) and the French ANR-PIA program (ANR-18-MPGA-0006). For permission to work and sample in P. N. Torres del Paine, K. C. is grateful to two Chilean agencies: Corporación Nacional Forestal (Resolución 15/2015), and Dirección Nacional de Fronteras y Límites del Estado. In the P. N. Los Glaciares (Fitz Roy massif), C. S. , and M. C. G. are greatful to the Administración de Parques Nacionales Argentina (permit 31-DRPA to M. C. G. ), and all the people who helped us on the field, specially the mountain guide Santiago Arias in El Calafate, Argentina.
The Université Grenoble Alpes, the French CNRS, the INSU SYSTER project, and the ECOS-SUD project A15U02 also supported this work. V. A. P. M. acknowledges the ERASMUS+ program for the mobility grant to visit the Université Grenoble Alpes, and the TRB team. P. G. V. acknowledges funding support from the Swiss National Science Foundation SNSF (Grant PP00P2_170559) and the French ANR-PIA program (ANR-18-MPGA-0006.
Here we use available legacy and modern multichannel seismic datasets to investigate the extensional features of the forearc in the Unimak and Shu-magin segments of the AASZ. Forearc extensional faults have been known for a long time to be present in the vicinity of trenches [e. g. Aubouin et al. , 1984]  in response to various factors including gravity combined with vertical motion, but also forearc stretching due to arc-parallel sliver motion in oblique  subduction [e. g. Avé Lallemant, 1996]. Our analysis suggests such a dual origin for forearc extension. We discuss the possible onset, or starting point, of Aleutian partitioning around the Sanak Island and interpret the 280-km-long, landward dipping, trench-parallel normal fault system from Unimak to Shumagin segments in terms of reactivation of terrane sutures and seismogenic behaviour of the shallow plate interface.
, 2011 , Li et al. , 2018 , Bécel et al. , 2017]. ALEUT Line 6 (Figure  6 ) is of particular interest since it is located at the junction of the Central and Eastern Sanak basins, in an area of poor coverage of the legacy data. The shelf break and slope section of Line 6 has been reprocessed using the CGG Geovation Seismic Imaging software. The processing workflow includes denoising, SRME and Radon multiple attenuation and finally Kirchhoff Prestack Time Migration [see  Liang et al. , 2019 , for more details on the processing workflow]. USGS Line 221 was available as a non- migrated stack but is presented here after application of a post-stack, water velocity Kirchhoff Migration (Figure  7 ). Streamer tomography (Supplementary Figure  S2 ), as published in  Bécel et al. [2017] , is also used to detect a basement high beneath the shelf (small yellow star on Figure  2 , 100 km from the trench in Figure  6 ).
In contrast, two landward-dipping normal faults are associated with the Miocene sediment wedges (just above basement in both cases). As a result, we favour a more recent activity of the seaward-dipping faults when compared to the landward-dipping faults. Down the slope, ALEUT line 6 features a large tilted block bounded by seaward-dipping growth normal faults and landward-dipping toe-thrust faults (Figure  6 ). These observations all point to a slope collapse posterior to the formation of the Sanak Basin. In the entire legacy and modern dataset, such a slope-collapse is observed in a limited area in the vicinity of the shelf break embayment (Figure  6 ), corresponding to the junction between the oblique Central Sanak Basin and the Eastern Sanak Basin.
These observations highlight that the so-called "oblique" Central Sanak basin does not only feature trench-oblique structures but also diffuse trench perpendicular structures. Another oblique structure, parallel to the ones in the Central Sanak basin, is inferred separating the Unimak basin from the Western Sanak basin in  Bruns et al. [1987]  (Figure  4 ). Multibeam bathymetry data that were not available in the 80's and now included in the GMRT v4. 0 dataset  [Ryan et al. , 2009] , show a clear offset of the Unimak ridge (Figure  4 ) separating it from the "Unimak Seamount", in the continuation of the fault inferred by  Bruns et al. [1987]. This offset could indicate transtensional faulting at the southwestern boundary of the "Sanak Island High" (Figure  8 ).