dataesr/scientific-paragraphs-categorization huggingface dataset:
This process was continued up to an axial strain of 0. 08-0. 12. This method of measuring permeability during deformation has been used previously on porous sandstones  (Baud et al. , 2012; Fortin et al. , 2005; Zhu & Wong, 1997)  and porous limestones  (Meng et al. , 2019) , allowing our new data for volcanic rocks to be easily compared with previously published data. We adopt the convention that compressive stresses and strains are positive. We performed an additional experiment in which we measured the porosity change and permeability of a sample during hydrostatic pressurization up to a P e of 150 MPa, using the same method described above.
First, we take the data for k(ϕ) for the samples in the brittle (20 < P e < 60 MPa) and ductile (90 < P e < 150 MPa) regimes and examine the permeability data for where Q < C′ and Q < C * , data for which the deformation is considered to be elastic. We also consider here data from the experiment in which permeability and porosity were measured during hydrostatic loading to a P e of 150 MPa (data also considered to be elastic, since P e < P * , where P * is the P e required for inelastic hydrostatic deformation). In this elastic regime, the data k(ϕ) are steep, and characterized by an apparent n that appears largely independent of P e and which takes a best-fit value n ≈ 47 (Figure  10a ). As discussed above, due to the low pre-existing microcrack density (Figure  2a ), we consider that permeability reductions during pressurization and loading in the elastic regime are the result of the closure or "pinching" of narrow pore throats that help connect the porosity backbone.
Conclusions In this study, we measured the evolution of porosity and permeability (in the direction of the maximum principal stress) of a porous volcanic rock during deformation in the brittle and ductile regimes. Although data of this type are available for porous sandstones and limestones, the data provided here are a first for porous volcanic rock. In the brittle regime, the permeability of Volvic trachyandesite decreases by a factor of 2-6 up to the peak stress due to the closure of preexisting microcracks but, following shear fracture formation, remained more-or-less constant as strain was accommodated by sliding on the resultant shear fracture (Figures  4  and 5 ). The absence of permeability changes upon shear fracture formation and during sliding on the fracture can be explained by the fact that the shear fractures did not connect the top and bottom of the samples (Figure  3d ).
We propose in this study to measure the siliciclastic sediment volumes in a retro-foreland basin where limited frontal accretion allows a more complete preservation of syn-tectonic deposits-the Aquitaine Basin and the Bay of Biscay during Cenozoic times for a better understanding of the erosion, the sediment transfer and deposition during the convergence to post-convergence periods of the Pyrenees Mountains and discuss at the first order the tectonic and climatic control factors. The measurement of the compacted siliciclastic sediment volumes (for a solid rocks equivalence) is based on sediment thickness (isopach) maps of known lithologies, built from an extensive dataset of seismic lines interpreted using the principles of seismic stratigraphy and dated on wells  (Ortiz et al. , 2020).
SILICICLASTIC SEDIMENT VOLUMES AND RATES The measurement of siliciclastic sediment (sink) volumes is based on four sediment thickness (isopach of preserved sediments) maps: Palaeocene-Eocene (66-33. 9 Ma-Figure  3 ), Oligocene (33. 9-23. 03 Ma-Figure  4 ), Miocene (23. 03-5. 3 Ma-Figure  5 ) and Pliocene-Pleistocene (5. 3-0 Ma-Figure  6 ). These isopach maps are the products of a seismic stratigraphic analysis of an extensive seismic line dataset (TotalEnergies, BRGM, BSS, Figure  1 ). This quite low time-resolution is due to the absence of wells in the deep Bay of Biscay and the difficulty to extend timelines from the Aquitaine Platform where several dated wells are available (see  Ortiz et al. , 2020). For each interval the main lithologies proportion is known in the Aquitaine platform and in the Landes Plateau (see  Ortiz et al.
We show that there is a need to investigate different SAR data products when estimating GH event timing (amplitude, spatial amplitude correlation, and coherence) since the signal response can be different and sometimes contradictory when looking at one single event. The implementation of our method on a cloud computing platform can be beneficial in terms of scalability, data availability and processing time. However, the main limitations in this context are:  (1)  no control in pre-processing of S1 imagery and, (2) S1 coherence data is so far not available within these platforms. With a focus on four events containing a total of about 2500 landslides and flash flood features in contrasting landscapes, we propose a method that is adapted to be applied to other regions. Here, we focused on tropical environments where climate conditions and land use dynamics are rather specific.
Acknowledgement This study was supported by the  Belgium Science Policy (BELSPO)  through the  PAStECA  project ( BR/165/A3/PASTECA ) entitled " Historical Aerial Photographs and Archives to Assess Environmental Changes in Central Africa " (http://pasteca. africamuseum. be/, last access 09 June 2022). The compilation of the inventory data benefited from field-based insight and discussion with  Arthur Depicker ,  Josué Mugisho Bachinyaga ,  John Sekajugo  and  Judith Uwihirwe. PlanetScope data provided by the  European Space Agency. Small, D. : Flattening gamma: Radiometric terrain correction for SAR imagery. IEEE Trans. Geosci. Remote Sens. , 49(8), 3081-3093, https://doi. org/10. 1109/TGRS. 2011. 2120616, 2011 Srivastava, H. S. , Patel, P. and Navalgund, R. R. : How far SAR has fulfilled its expectation for soil moisture retrieval.
Conceptual drilling and coring strategy We have identified three primary and five alternative sites on seismic lines in the northern Aegean (AEG-01A and AEG-02A), the Sea of Marmara (MAR-01A and MAR-02A), and the Black Sea basin (BSB-01A, BSB-02A, BUL-01A, and BUL-02A). Core recovery must be sufficient for highresolution sampling with minimal gaps. Therefore, we propose the use of an advanced piston corer (APC) to refusal at each site, followed by a rotary core barrel (RCB). Limited core recovery in the single/double sites will be mitigated by the acquisition of downhole logs under open-hole conditions (see below). These data will also be used to generate comprehensive cyclostratigraphic records. More detailed information on the sites used is given in the following: -Aegean -primary site is the North Aegean Trough (AEG-01 with ∼ 650 m penetration; one hole down to 650 m and one hole down to 100 m), yielding a total expected core recovery of 750 m, and the alternative site is AEG-02, which involves a lateral shift in location that shows smaller stratigraphic thickness; -Sea of Marmara -preferred site is the North İmrali (MAR-01; one hole down to 400 m), and the alternative site is the MAR-02, which involves a lateral shift in location that shows smaller stratigraphic thickness; and Sci.
Acknowledgements. The authors wish to thank the  Senckenberg Biodiversity and Climate Research Centre in Frankfurt  (in particular  Andreas Mulch ),  Germany , for hosting the event and  Iryna Yashchenko  and  Tjitske Vos  for their managerial support and assistance. We are also grateful to  Lucas Lourens  for continued encouragement and constructive suggestions and to  Nadine Hallmann  and  Gilbert Camoin  for essential hands-on support with respect to organizing the workshop. Finally, we acknowledge all participants for their constructive input and enthusiasm. Those interested in participating in future BlackGate activities are invited to contact the authors. Financial support. This research has been supported by  ECORD/IODP  ( BlackGate2020 grant ); the  US Science Advisory.
The swath width was 513-741 m, with an overlap of 55-70 percent. The average density of total returns (including vegetation) was 48. 39 points/m 2 in Phase I and 39. 64 points/m 2 in Phase II, while the ground return density (Grtn) was 2. 18 points/m 2 in Phase I and 2. 95 Grtn/m 2 in Phase II. The LiDAR point data were delivered to FARES in LAS 1. 2 in 500 m 2 tiles. Post processing of the Phase I survey with Rapidlasso's LASTools software provided a ground density return of 5. 2 Grtn/m 2. The overall accuracy of both surveys is +/-15 cm horizontal and +/-30 cm vertical. QuickTerrain Modeler was used to create bare-earth digital elevation model (DEM) and digital terrain models (DTM) with a 0. 5 m resolution. Once the LiDAR-derived DEM was generated, we produced different surface and visualization models to interpret archaeological features, including hillshade with different light positions.
Hillshade models have been widely applied in archaeology in tropical environments to enhance, detect, and define cultural remains (A. S. Z. Chase et al. 2017; Chase et al. 2014; Dunning et al. 2019; Evans et al. 2013; Golden et al. 2021; Horn and Ford 2019; Rosenswig and López-Torrijos 2018; Šprajc et al. 2021; Thompson 2020 ). To generate visualizations and interpret archaeological features, we used several software programs, including RVT, ArcMap, GlobalMapper, Quick Terrain Modeler, and QGIS.
This feature is 30-40 m wide and 2-4 m high, and extends 7. 4 km to a semirectangular aperture in the terrain of the natural topography before continuing on another 2. 3 km to the northeast Mexican border. There is a likely possibility that this causeway extends towards Yaxnohcah or Chicanticanal in Campeche, and not Calakmul, as purported earlier  (Folan et al. 2001:296-297). At present, there is no indication on LiDAR data of a causeway between El Mirador and Calakmul, which is logical considering the differences in contemporaneity of the sites, even though Calakmul does have some Preclassic occupation and at least one monumental substructure. An important causeway (Mirador-Nakbe causeway) extends from the southeast corner of the second platform of Danta pyramid, 13 km to the site of Nakbe.
Radiocarbon years were calibrated to calendar years using Calib 7. 0  (Stuiver and Reimer 1993)  and the IntCal13 dataset  (Reimer et al. 2013)  period, but certainly by the beginning of the Late Preclassic period (Figure  19 ;  Hernández-Salazar 2021:152-154, 60 ff. ; Hernández et al. 2016; Schreiner and Hernández 2009; Schreiner et al. 2015). Calculations of the volume of the Tintal-Mirador causeway, based on excavations, determined that the Preclassic Maya used as much as 10,000 m 3 /km of lime plaster and lime reinforced fill for elevated sections of the causeway. Schreiner and Hernández also determined that up to 40,000 m 3 /km of tzaal stone (a soft, porous limestone of nearly pure calcium carbonate, with 2 percent montmorillonite clay) was used on the combined volume of the four sequential renovations of the causeway  (Hansen 2012b:263-264; Hansen et al.
Introduction To date, more than 240 different species have been identified in space in the gas phase  [1]. Since gas-phase reaction rates are often found to be too low to account for the observed abundances of species in space, the icy mantles of interstellar dust grains are believed to give rise to a rich prebiotic chemistry, which feeds complex organic molecules (COMs) to star-forming regions and ultimately to planetary systems  [2, 3, 4]. Current infrared (IR) observations show that laboratory spectral data on peak position and feature width can be used to extract information on layering and mixing of interstellar ices  [5, 6]. The NASA James Webb Space Telescope (JWST) mission will enable the observation of interstellar ices over a wide wavelength range (0. 6-28. 3 m) toward a large variety of sources.
2-15. 2 m). All irradiations of pure CO 2 ice deposited at 20 K and at 75 K are carried out for five minutes to ensure the complete saturation of any structural changes in the ice. The spectral FWHM of the FELIX beam is on the order of 0. 8 % ∕ for all wavelengths. Unless otherwise specified, the laser macropulse energy at longer wavelengths (∼130 mJ in the 15 m wavelength region) is attenuated to ∼20 mJ to match that in the 3-4 m region. Thus, at all wavelengths investigated, the average power is ∼0. 03 W, with a laser fluence at the sample of approximately ∼0. 2 J/cm 2. Table  1  shows the main experiments and their FEL irradiation details. FTIR spectra are acquired before and after irradiation, from which difference spectra are obtained to highlight changes in the IR band profiles. All data analysis and spectral manipulation is performed using in house python scripts.
FEL-induced photodesorption could contribute to the observed reduction in the 2 -mode intensity upon irradiation. However, we should not exclude other possibilities such as hole-burning effects, particularly at the irradiated frequencies. Here, QMS data is key to directly detect FEL-induced photodesorption of CO 2. Unfortunately, although QMS data were successfully recorded during ice deposition and TPD experiments, during FEL irradiation, the acquisition speed of the instrument was not optimized for the detection of gas desorption plumes ejected from the ice in short bursts due to the pulsed nature of the FEL. Hence, during FEL irradiation, QMS results were inconclusive. The issue is beyond the scope of this paper and it will be addressed in future work. As for the case of pASW  [15] , all morphological changes in the CO 2 ice are localized within the area exposed to the laser beam and do not cause a global effect throughout the ice.
Acknowledgements The authors thank the  HFML-FELIX Laboratory team  for their experimental assistance and scientific support. The LISA end station is designed, constructed, and managed at the  HFML-FELIX Laboratory by the group of S. Ioppolo. This work was supported by the  Royal Society   University Research Fellowships Renewals 2019  ( URF/R/191018 ); the  Royal Society   University Research Fellowship  ( UF130409 ); the  Royal Society   Research Fellow Enhancement Award  ( RGF/EA/180306 ); and the  Royal Society   Research Grant  ( RSG/R1/180418 ). Travel support was granted by the  UK Engineering and Physical Sciences Research Council (UK EPSRC  Grant  EP/R007926/1  - FLUENCE: Felix Light  for the UK: Exploiting Novel Characteristics and Expertise).
These settings were optimized before the start of the campaign and checked throughout the campaign using standard VOC mixtures diluted with an Ionicon Analytik gas calibration unit (GCU) at 70% relative humidity and 25°C. Three different standard VOC mixtures (containing among others trans-but-2-ene, but-1-ene, and cis-but-2-ene) were used for optimisation and calibration of the instrumental signals (Text S2 in Supporting Information S1). During the campaign, spectra were integrated over 5 min and blank measurements were done at ambient relative humidity three times per day using the catalytic converter of the GCU to subtract potential contaminations from the sampling lines. Data analysis was done using GRAMS/AI version 9. 3. VOC concentrations were obtained by external calibration for compounds for which gas standards were available or estimated based on the rate constant of the proton-transfer reaction from H 3 O + only, or from both H 3 O + and (H 2 O)H 3 O +  (Ellis & Mayhew, 2014) , depending on the proton affinity of the compound, whenever identification was possible.
Aerosol Size Distributions Ambient aerosol number size distribution data from 10 nm to 30 μm were obtained by a combination of standard optical and electrical mobility analyzers. The aerosol number size distribution from 10. 9 to 461. 4 nm in diameter was measured by a Scanning Mobility Particle Sizer (SMPS), comprising of a Differential Mobility Analyzer (DMA, model 3,080, TSI Inc. , Shoreview, MN) and a Condensation Particle Counter (CPC, model 3,772, TSI Inc. , Shoreview, MN) operated at 1. 0/5. 0 L min -1 aerosol/sheath flow rate on a 3-min averaging time, including 2. 5 min of sampling of the size distribution data (scan up period) and 30 s scan retrace time period. The SMPS operated from a certified Total Suspended Particulate (TSP) sampling head (Rupprecht and Patashnick, Albany, NY, USA), followed by a cyclone impactor cutting off aerosol particles larger than 1 μm in aerodynamic diameter (using a flow rate of 16 L min -1 ).
These corrections were implemented using the Particle Loss Calculator program developed by Von Der  Weiden et al. (2009). Based on the measured dimensions of the sampling lines, the campaign-average wind speed of 6 L min -1 , and the equivalent sphere aerodynamic diameter (D a ) estimated from D g as 𝐴𝐴 𝐴𝐴𝑎𝑎 = 𝐴𝐴𝑔𝑔 √ 𝜌𝜌𝑝𝑝∕𝜌𝜌0 , where ρ p is the ambient particle mass density and ρ o is the unit reference particle mass density. Finally, in order to merge the measured SMPS and GRIMM OPC size distributions, an iterative approach was implemented. The physical aerosol parameters (χ, m, ρ) were varied until the size-dependent loss corrected SMPS and GRIMM OPC size distributions agreed on their nominal overlap region (0. 25-0. 46 nm). The best agreement was obtained with the following average values: χ = 1 and m = 1.
Aerosol Composition Online aerosol composition was measured using a compact-Time-of-Flight Aerosol Mass Spectrometer (c-ToF-AMS), providing a comprehensive chemical composition of non-refractory PM 1. Data used here were analyzed using the Igor Pro package, Squirrel (version 1. 63G), and cumulative peak fitting analysis according to the method described in  Müller et al. (2011). Calibration was performed on-site before and after the campaign using ammonium nitrate, ammonium sulfate, sodium chloride, and polystyrene latex spheres. Size-dependent aerodynamic lens transmission efficiency was 30% at 60 nm, 60% at 70 nm, 100% between 80 and 550 nm, 60% at 600 nm, 50% at 700 nm, and 30% at 900 nm  (Liu et al. , 2007). Analysis of the composition of nebulized ocean water was used to calculate the sea-salt sulfate (ss-SO 4 2- ) and non-sea-salt sulfate (nss-SO 4 2-) fractions based on the measured sulfate-to-chloride ratio.
Statistical Analysis Hierarchical cluster analysis, to compare ambient mass spectra during VOCs peak events with reference mass spectra of ocean foam and water (raw spectra, PTR-ToF-MS), were done using the Euclidean distance (based on peak intensities in counts-per-second), single linkage method in Statsoft Statistica 8. 0. All correlations were done based on r-Pearson using Microsoft Excel 2016. Lagged correlations were done using the "ccf" function in the "tseries" package in R studio (R version 3. 4. 1). For statistical significance we used a 95% confidence level. Correlation strength was defined using the guidelines of  Cohen (1988). Unless otherwise stated, correlations were done on data covering the entire campaign.
Conflict of Interest The authors declare no conflicts of interest relevant to this study. for assistance with the calculations of condensational growth rates and nucleation rates and with the use of the PARGAN codes. The authors wish to thank Edouard Pangui (LISA) for his technical support during the field campaign preparation and AERIS (https:// www. aeris-data. fr/), the French centre for atmospheric data and service, for providing the campaign website and organising the curation and open distribution of Aerosols, Radiation and Clouds in southern Africa (AEROCLO-sA) data. Authors are grateful to the AEROC-LO-sA consortium for their work in the field and during the preparation of the field campaign, and Sam Nujoma Marine and Coastal Resources Research Centre for hosting the field campaign.
The MicMac routines 'tapioca', 'tapas', 'GCPBascule', 'Campari' and 'Malt' perform the sequence of steps needed in the photogrammetric processing, consisting of the computation of tie point generation, solving of relative and absolute image orientation, and performing the dense matching and creation of the DEM and orthoimages. The processing is semi-automated: a series of 23  GCPs (1984) and 28 GCPs (1962)  were manually digitized in the 2020 Pléiades orthoimage and in the corresponding pairs or triplet of aerial photographs (see Fig. S1 ). The elevation of each GCP was extracted from the 2020 Pléiades DEM. This scheme had been previously used by  Papasodoro and others (2015) , and resulted in photogrammetric DEMs and orthomosaics co-registered to the Pléiades 2020 dataset.
Journal of Glaciology glaciers, Manchana Covunco being the largest one (1. 7 ± 0. 1 km 2 ). Still, from 1962 to 2020, we report area and mass changes for the ten largest glaciers (>0. 5 km 2 ) which total 22. 6 km 2 in 1984, i. e. 78% of the total glacier area. Surface conditions (cloud and snow cover) allowed for the clear delineation of glacier margins in the 1984 aerial photos, the 2003 ASTER images and Pléiades 2020 scenes. The Pléiades 2012 scene and 1962 aerial photos do nevertheless display a slight amount of seasonal snow. In the first of these two cases, glacier mapping was performed with the aid of a WorldView-2 4th April 2012 image available from GoogleEarth with very dry conditions. Finding an alternative dataset that can be used to validate the 1962 glacier outlines is far more problematic.
Comparison of DEMs with in situ global navigation satellite system (GNSS) measurements Validation of all DEMs, except for DEM 1962 , was carried out by comparing field-surveyed check points (CPs) off glacier against each DEM (Fig. S1 ). This was not possible for DEM 1962 because the buffered coverage (for DEM co-registration purposes) around individual glaciers did not coincide with CPs (see Section 3. 4). A total of 14 CPs were surveyed during field campaigns in 2012 and 2016 using Trimble 5700 receivers and spanning 2400-3800 m a. s. l. in elevation. CP coordinates were differentially postprocessed using data from the Chos Malal GNSS continuous station (37°22 ′ S-70°16 ′ W, 875 m, ellips. ). The mean horizontal and vertical precision of these CPs were 0. 02 and 0. 06 m, respectively. First, we determined the offset of the most recent DEM 2020 relative to the CPs.
Analysis of climate records We analysed summer (October-March) air temperatures and winter (April-September) precipitation records available from the Pampa de Chacaico meteorological station (36°28 ′ 56. 4 ′′ S, 70°3 6 ′ 9. 3 ′′ W, 2580 m a. s. l. ), located 17 km north of Domuyo. Monthly data from this station were available between 1997 and 2010. These records closely reflect the climate conditions at Domuyo, as shown when monthly temperature and precipitation records from Pampa de Chacaico are compared with ERA5 reanalysis data using the KNMI climate explorer platform (www. climexp. knmi. nl). Both the temperature and precipitation records from Pampa de Chacaico depict a far-reaching spatial correlation field with r > 0. 6 over the Central and Northern Patagonian Andes between ∼31°S and 43°S (Fig.
2 ). We extended the monthly time series of air temperature and precipitation at Pampa de Chacaico using ERA5-Land reanalysis data for the period between 1981 and 2020. ERA5-Land is an enhanced dataset derived from ERA5 for the land component (Muñoz-  Sabater and others, 2021). We corrected the ERA5-Land data at the location of Pampa del Chacaico through a linear regression, using the meteorological observations available for the 1997-2010 period and ERA5-Land outputs for the same period. Regression models are a simple, appropriate and straightforward method to apply for monthly temperature considering the linearity of the relationship and the normal distribution (  Wilby and others, 2004 ). An RMSE of 0. 9°C was obtained after the correction. The regression parameters were used to bias-adjust the ERA5-Land time series for the entirety of the analysed period.