dataesr/scientific-paragraphs-categorization huggingface dataset:
A pOsterIOrI morphological re-inveStigation After the species delimitation and phylogenetic analysis, new morphological investigations were performed to clarify the mismatch between morphological and molecular data and the status of ambiguous taxa. For unrecognized molecular units, new discriminant morphological characters were potentially identified. First, we find a different number of marginal oral spines (five vs. three) in two genetic entities initially identified under the name P. affinis (i. e. P. jordani/ affinis and P. militaris/affinis). Second, the presence of a large, clavate suboral spine is found in several specimens of the Diplopteraster/P. stellifer complex, all belonging to P. stellifer unit 1 and P. stellifer unit 5. Third, the morphological re-examination of two closely related molecular units (P.
ACKNOWLEDGEMENTS This work was supported by the  'Refugia and Ecosystem Tolerance in the Southern Ocean ' project (RECTO;  BR/154/A1/RECTO ) funded by the  'Belgian Science Policy Office' (BELSPO). This is contribution no. 15  to the  RECTO  project. We thank  Guillaume Achaz ,  Sylvain Bouquin ,  Marc Eléaume ,  Bruno Frédérich ,  Christopher Mah ,  Sadie Mills ,  Kate Neil ,  Philippe Pernet ,  Chester J. Sands  and  Régine Vignes-Lebbe  for their precious help and advice. We thank the two anonymous reviewers for their pertinent comments. We thank the captains, crews and scientists who contributed to the material collected from the  Royal Research Ship James Clark Ross  ( JR144 ,  JR179 ,  JR262 ,  JR275  and  JR15005 ),  RV Polarstern  ( ANDEEP-3 ,  ANDEEP-SYSTCO ,  PS77 ,  PS81  and  PS96 ),  Akademik Treshnikov  ( Antarctic Circumnavigation Expedition, Swiss polar Institute ), FV Austral (Poker 2, principal investigator Guy Duhamel),  Aurora Australis  ( CEAMARC 2007 ( CEAMARC -2008 )),  N.
O. Alis  ( MUSORSTOM 10 ),  Marion Dufresne  ( MD 208 ) and the  ARGOS program. Photographs of H. escourti and P. bathami in the identification key were provided by the  National Institute of Water and Atmospheric Research (NIWA) Invertebrate Collection  and were taken on R/V Tangaroa on a variety of research voyages, including:  TAN0413 , Bay of Plenty Seamounts voyage part of the project 'Seamounts: their importance to fisheries and marine ecosystems', undertaken by  NIWA  and funded by the  New Zealand Foundation for Research, Science and Technology  with additional funding from the  New Zealand Ministry of Fisheries  (MFish, now FNZ) and  NOAA Satellite Operations Facility ; and  TAN1116 ,  Fisheries Oceanography  voyage supported by the  New Zealand government  under 'Coasts & Oceans' core funding from the  Ministry of Business, Innovation and Employment , Project:  Food-web dynamics of New Zealand marine ecosystems.
Observation of the spurious phase We correlate all of the available pairs of processed noise segments and stack them to produce the correlation function of the year-long data for each FNET-LAPNET station pair. A diagram showing the computation of the correlation function is is found in Fig. S1  in the Supplement. The correlation function contains a causal part and an acausal part that correspond to the positive and negative time lags respectively. In this paper, the acausal correlations correspond to seismic waves that travel from FNET to LAPNET (causal: from LAPNET to FNET). The noise correlations of all of the FNET-LAPNET station pairs are binned in an inter-station distance interval of 0. 1 • , to produce the waveform sections for the acausal and causal parts of the noise correlations. The filtered sections (periods of 5 to 10 s) of the vertical-vertical noise correlations are shown in Fig.
4  and the broadband sections in Fig. S2. The theoretical P and PcP waves marked on the panels are predicted using the TauP program  (Crotwell et al. , 1999)  and the IASP91 Earth model  (Kennett and Engdahl, 1991). A coherent arrival between 410 and 450 s is clearly visible in the acausal section of noise correlations, about 200 s earlier than the direct P wave that should be the primary arrival. The early arrival has no correspondence in the true Green's function of the Earth medium, and thereby is undoubtedly a spurious phase. Spectral analysis indicates that the spurious phase has a peak period of 6. 2 s (Fig. S3 ), typical for secondary microseisms. As estimated from the acausal vespagram in Fig. 4 , the emerging time and apparent slowness of the spurious phase at 63 • distance are about 430 s and 4.
The spurious phase is observable in the acausal correlations because the corresponding source is strong, and is hardly observable in the causal correlations because the responsible source is too weak. It is worth confirming whether the spurious phase can be eliminated with an ideally uniform source distribution or not. We request the vertical components of the synthetic global broadband seismogram for the iasp91_2s model from the IRIS Syngine Data Service  (Krischer et al. , 2017)  powered by the spectral-element program AxiSEM  (Nissen-Meyer et al. , 2014)  and the Python packages Obspy  (Krischer et al. , 2015)  and Instaseis  (Van Driel et al. , 2015). A mask is applied to the full waveforms (Fig. 10a ) to extract the P waves and the PKPab waves (Fig. 10b ). Providing that the uncorrelated noise sources are distributed evenly on the global surface, we compute the source-wise correlations and stack them for each inter-station distance, using the data in Fig.
resif. fr, last access: 30 June 2018) respectively. The global earthquake seismograms were obtained from the IRIS GlobalStacks Data Ser-vice (https://doi. org/10. 17611/DP/GS. 1, IRIS-DMC, 2014). The global synthetic seismograms were obtained from the IRIS Syngine Data Service (https://doi. org/10. 17611/DP/SYNGINE. 1, IRIS-DMC, 2015). The data of synthetic global microseism noise sources were provided by the IOWAGA products  (Rascle and Ardhuin, 2013). The TauP program  (Crotwell et al. , 1999)  and the IASP91 Earth model  (Kennett and Engdahl, 1991)  were used to calculate the theoretical travel times and ray parameters of seismic phases. Supplement. The supplement related to this article is available online at: https://doi. org/10. 5194/se-11-173-2020-supplement. Author contributions. LL performed data processing and designed the synthetic experiments.
Acknowledgements. The computations were performed with the CIMENT cluster (https://ciment. ujf-grenoble. fr, last access: 27 September 2018), which is supported by the  Rhône-Alpes  grant  CPER07_13   CIRA. The authors acknowledge the constructive reviews of  Pilar Sánchez-Pastor  and an anonymous reviewer. We also thank  Sidao Ni  for his comments and suggestions on an early draft that improved the manuscript. Financial support. This research has been supported by the  Labex   OSUG@2020 (Investissements d'avenir-ANR10LABX56 ) and the  la Fondation Simone et Cino Del Duca, Institut de France  (Prix scientifique 2013). Review statement. This paper was edited by  Irene Bianchi  and reviewed by  Pilar Sánchez Sánchez-Pastor  and one anonymous referee.
Optical imagery Landsat-8 and Sentinel-2 georeferenced RGB colour composite images were downloaded from 235 the USGS data portal (https://earthexplorer. usgs. gov/). The images were used for 1) precise selection of the Jason measurements over the river channels at corss-overs and 2) demonstration of the spatial heterogeneity of the ice phenology between satellite-river cross-overs (virtual stations or VS). The ice season corresponds to the low-flow period, when the river width is minimal. Considering 240 this, for the first task, images acquired on 2 August 2013 (end of the flood recession) and 18 October 2013 (beginning of the winter low-flow) were used. This helped to minimize the impact of land contamination when selecting the altimetric measurements.
Terrestrial 10 Be erosion rates The concentration of 10 Be in quartz hosted in ridgeline soils and river sediments provides hillslope erosion rates integrated over the past 10 3 -10 4 years (Appendix B). The soils and rocks collected along ridgelines located in the SM range provide site-specific erosion rates (Table  S2 -1, Fig. S2-3c ). They consist of crushed and amalgamated quartzose vein fragments hosted in weathered orthogneiss (3 samples), and of single blocks of highly weathered pegmatite from the Cerro las Palomas, a monadnock located on the Montaña El Imposible (2 samples). The majority of the dataset, however, consist of 10 Be concentration measured in riverborne quartz, collected in rivers that drain the SM, SC, and AC ranges. They provide catchment-averaged estimates of soil erosion rate  (Brown et al.
4. River profile segmentation To study the response of stream incision to uplift, particularly in the form of upstream-migrating waves of accelerated or decelerated incision, we extracted the long-profiles of 220 rivers draining the AC, SC, and SM ranges from the Guatemala national 20 m-resolution DEM, released by the National Geographic Institute of Guatemala. Karstic processes, debris flows, and deep-seated landslides dominate the evolution of many small streams, which were therefore excluded from the dataset. A subset of 110 rivers that better capture the evolution of the overall landscape was used in the final analysis (Fig. 7 ). https://doi. org/10. 5194/esurf-2020-80 Preprint. Discussion started: 9 November 2020 c Author(s) 2020. CC BY 4. 0 License. River gradients decrease steadily in the downstream direction due to the increase in river discharge.
High-pass filtering improved the signal to noise ratio by eliminating the components lower than 2 Hz that are not propagated in the SOFAR channel. A correction taking into account the difference in travel time in the liquid and solid mediums was finally applied using a refined model of Hawaii  (Hill, 1969; Watts and ten Brink, 1989). Two locations were finally obtained: The precision of the latter location was investigated through a Monte Carlo algorithm by carrying out a large number of relocations after injecting Gaussian noise with standard deviation σG into the dataset. We took σG = 1. 3 corresponding to the standard deviation of the residuals broad value taking into account the quality of the data and association of Pg, Pn, P and T phases. The results for 1,000 iterations are shown in figure  5.
Hydroacoustic data Together with the channelling efficiency of the Sound Fixing and Ranging (SOFAR) channel, the all but negligible anelastic attenuation in the water column makes for an exceptionally efficient transmission of T phase energy at teleseismic distances and thus results in superb detection capabilities  (Talandier and Okal, 1998; 2016)  ) for natural or artificial explosions, earthquakes, volcanic activity  (Talandier and Okal, 1984; 1987) , hydrothermal activity  (Talandier and Okal, 1996)  and iceberg drifting  (Talandier et al. , 2002; 2006). In such cases, T phases can be recorded either by island seismic stations after conversion of the acoustic wave to seismic wave on the underwater slopes or by hydrophones wetted in the SOFAR channel. In this paper, all displayed records were corrected for the instrumental response and a high-pass filter improving the signal/noise ratio by eliminating the components lower than 2 Hz that are not propagated in the SOFAR channel.
In the frequency domain, we use several methods including the study of the decay of spectral amplitude with frequency (both in terms of a power law, and of smoothness), and the evolution of the duration of the signal when corrected using an empirical compensation of any frequency dispersion present in its Fourier spectrum. The combination of these methods provides a precise identification of the nature of all sources with reference to a large dataset of more than 300 signals. The paroxysmal explosion of May 29th, 2010 at South Sarigan is exceptional because of its energy and the fact that it affected at the same time solid, liquid and subaerial media. Therefore, it gives us the opportunity to apply these criteria to the T phases of South Sarigan recorded by the Wake hydrophone H11N1 and KNTN seismic station.
The width of the South Sarigan T phase envelope is smaller than that of the artificial reference envelope and its amplitude growth (red dotted line) is clearly faster. Therefore, the source of the South-Sarigan event is typically explosive and at least as impulsive and fast as those of artificial underwater explosions. (d) Study of the decay of spectral amplitude with frequency  (Reymond et al. , 2003) : Both in terms of a power law r² and of smoothness , earthquakes and explosions can be discriminated on the basis of the variation with frequency of the spectral amplitude of ground velocity. A dataset of 206 records indicates that for most explosions < 1. 4, while most earthquakes have > 1. 5. Moreover, the correlation coefficient r² is generally smaller than 0. 7 for most explosions, and greater than 0.
72. This could imply an underestimation of our result by a factor of 2 or 3. Moreover, the young and shallow andesitic volcanic bedrock of South Sarigan is probably more heterogeneous and less coherent than those of nuclear test sites, a feature that moves in the same direction. Finally, the proposed estimate relates only to the portion of released energy corresponding to the observed seismic effects. It does not take into account the hydroacoustic effects and the violent ejection of materials into the water column and the atmosphere. The charge (Cha) is in kg of equivalent TNT, the amplitude (Amp) in μm/s peak to peak normalized at a distance of 3000 km and (Pro) the depth of the explosion in m. However, if the coefficient c1 characterizing the slope of the regression line is well defined, conversely, depending on the dataset used, the coefficient c2 can be scattered.
The planation surfaces display gentle slopes (< 1°) over large areas, thus the elevation distribution is much smaller. A tiny deformation will modify the surface slope and widens the elevation distribution (Fig. 3b ). The widening of the distribution is directly relative to the amount of tilting or bending: the higher the deformation the greater the widening. Thus, the elevation distribution is a pertinent proxy for detecting a long wavelength deformation affecting a planation surface. Planation surfaces were mapped with GIS software using DEM (STRM 30), satellite images (SPOT) and observations made during field trips. Surface heights (Fig. 4 ) were mapped and their main characteristics are summarized in Table  2. The major challenge for constraining the landscape growth is the dating of the planation surfaces  (Watchman and Twidale, 2002).
, 2020). The late Artinskian to mid-Kungurian (upper Rotliegend I;  Kiersnowski, 2013)  age of the lower Salagou Formation (Octon Member) is well constrained by U-Pb ID-TIMS dates from ash layers  (Michel et al. , 2015 ; Figure  2 ). Chronostratigraphic constraints for the top of the formation (Merifons Member) are lacking, so the extent of Guadalupian deposition (cf. Schneider et al. , 2006; Pochat and Van Den Driessche, 2011)  is unclear. The Octon Member (basal to mid-upper Salagou) makes up the majority of the Salagou Formation and consists primarily of massive red mudstone with loessitic characteristics  (Pfeifer et al. , 2020). The MS data for this study were collected from the Octon Member to lower Merifons Member (Figures 1, 2; red bar), which represents deposition through the mid-late Cisuralian.
Time Series Analysis and Modeling Time series analysis of the MS stratigraphic series was carried out in MATLAB and Astrochron for R  (Meyers, 2014)  (see Supplementary Appendix S1 for commands). MATLAB functions were used to display the stratigraphic series, and for spectral analysis and evolutionary spectrograms to assess the distribution of variability as a function of frequency (cycles/meter) and along stratigraphic position to assess potential changes in sedimentation rate. A low-pass Taner filter was applied Permian Cisuralian Guadalupian Lopin. FIGURE 2 | A summary of the current Permian chronostratigraphic constraints of the Salagou Formation (Lodève Basin). The section where MS data were measured in this study is highlighted in gray and also indicated with the red bar. Note that the upper age of the Salagou Formation is very poorly constrained.
Sedimentology The correlation between MS measured in the field to χlf is weak (r 2 = 0. 1758), but the relationship between the two datasets is highly significant (P-value < 0. 05). (∼10+ cm), randomly oriented, semi-radial slickensides (Figures  3B, C ). Micromorphologic attributes of samples from these localities include higher proportions of clay, wedgeshaped peds, clay coatings on grains, and porphyroskelic fabrics. Geochemical analyses reveal elevated chemical index of alteration (CIA) values from these intervals (compared to neighboring loessite). These features, together with a lack of horizonation, are most analogous to modern Vertisols which are typically indicative of environments with seasonal precipitation (e. g. ,  Mack et al. , 1993).
Magnetic Susceptibility Measurements by KT-10 Table  2  summarizes the statistics of MS data obtained by portable MS meter, reporting the mean and standard deviation of susceptibility readings overall and by section (#1-9; Figure  3A ). Overall, the mean measurement of k (MS) for the Salagou formation is 0. 253 ± 0. 100 (×10 -3 ). The section with the lowest readings (uppermost Salagou; Section 9) averages 0. 179 ± 0. 034 (×10 -3 ) and the section with the highest readings (middle Salagou; Section 5) averages 0. 366 ± 0. 092 (×10 -3 ). This table reports the mean and standard deviation of MS measurements overall, and also by section (#1-9; corresponding with the stratigraphic columns in Figure  3A ). The number of readings (measurements) for each section is also reported, as well as the sampling interval.
The well-defined alignment of χlf and χ between these datasets (Figure  7 ) strongly suggests that the magnetic signal in the Salagou Formation is driven by pedogenesis. If there is no postdepositional (diagenetic) conversion of magnetite/maghemite to hematite, then the low contribution of magnetite in the Salagou Formation loess compared to Eurasian Quaternary loess might reflect substantially different paleoclimatic settings in the Permian of France. If changes in the magnetic signal are pedogenically driven, then samples in this dataset represent a range of pedogenic alteration, where samples with more magnetic enhancement are more enriched in ultrafine particles of hematite. However, the average bulk χ from interpreted paleosol (1. 3 ± 0. 3 × 10 -3 ) and loess (1. 5 ± 0. 4 × 10 -3 ) units in the Salagou Formation overlap within error.
4 cm/kyr (lower Salagou) and 13 cm/kyr (mid-upper Salagou). The up-section increase of optimal (ASM-based) sedimentation rates from 9. 4 to 13 cm/kyr suggests that the Salagou Formation represents a duration of 9-10 Myr. This result is similar to estimates for the Salagou Formation from previous work (11-17 cm/kyr; Pochat and Van Den Driessche, 2011) as well as average sedimentation rates for the middle Permian Lucaogou Formation of northwest China (8. 9-10. 3 cm/kyr;  Huang et al. , 2020). It is slightly faster than lower Permian loess deposition in western equatorial Pangea (>700 m over ∼9 Myr so ≥7. 8 cm/kyr;  Johnson, 1989; Tramp et al. , 2004; Soreghan M. J. et al. , 2014) , and on the lower end of sedimentation rates proposed for the Plio-Pleistocene CLP  (Stevens and Lu, 2009). If the driver of magnetic enhancement is pedogenesis (see section "Origin of the Magnetic Signal and Comparison to Quaternary Eurasian Loess"), then these data demonstrate fluctuation between loess accumulation and soil formation with loessite-paleosol couplets around 10 m thick in the Salagou Formation, which is similar to the lower Permian loessite of western equatorial Pangaea  (Soreghan M.
Note the pedogenic interval ∼11 m. The correlation between MS measured in the field to χlf is negligible (r 2 = 0. 0059), but the relationship between the two datasets is highly significant (P-value < 0. 05). (C) A 10-m section sampled at 30-cm intervals. Note the pedogenic interval ∼3-5 m. The correlation between MS measured in the field to χlf is weak (r 2 = 0. 1758), but the relationship between the two datasets is highly significant (P-value < 0. 05).
ACKNOWLEDGMENTS We thank  M. J. Soreghan  for suggesting collection of handheld MS data and our 2018 NSF IRES student participants for assistance with data collection ( L. Alaniz ,  E. Simpson ,  V. Smith , and  K. Yeager ). We thank  Stephane Pochat  and  Jean Van Den Driessche  for field assistance and collaboration. We thank  Kathrin Worm  for support in the magnetic laboratory. This is IPGP contribution number  4143. Thank you to reviewers RZ and DJ, and editor HA.
(B) An 80-m section sampled at 5-m intervals. Note the pedogenic interval ∼11 m. The correlation between MS measured in the field to χlf is negligible (r 2 = 0. 0059), but the relationship between the two datasets is highly significant (P-value < 0. 05). (C) A 10-m section sampled at 30-cm intervals. Note the pedogenic interval ∼3-5 m. The correlation between MS measured in the field to χlf is weak (r 2 = 0. 1758), but the relationship between the two datasets is highly significant (P-value < 0. 05).
The composition of the high pressure fluids (wt% cations dissolved) and melts (wt% H 2 O) was determined from available solubility studies (Table  2 ) as follows. The water content of haplogranite melts at equilibrium with aqueous fluids (Fig. 1B ) was calculated from the water solubility data for aluminosilicate melts reported by  Mysen and Wheeler (2000)  and extended to our experimental conditions. The composition of the aqueous fluids in equilibrium with the haplogranite melts (i. e. , total silicates content including SiO 2 , Al 2 O 3 , Na 2 O and K 2 O) was calculated, by extrapolating up to the P-T conditions of our experiments, the solubility data reported in the albite-H 2 O system between 0. 20 and 0. 84 GPa at 600 and 700 °C  (Anderson and Burnham, 1983). The composition of the hydrosilicate liquids in the NS2-H 2 O system was determined from the initial volumetric proportions of the NS2 glass and the aqueous fluid loaded in the compression chamber.
In-situ SXRF/XAS measurements and data analysis The SXRF and XAS measurements were performed at the MicroXAS beamline (X05-LA) of the Swiss Light Source (SLS, Paul Scherrer Institute,  Borca et al. , 2009). Measurements at the Br K-edge were conducted with an incident energy of 13. 6 keV tuned by a Si(111) double crystal monochromator and focused down to 5 x 8 (V×H) μm 2 size by a set of Rh-coated Kirkpatrick-Baez mirrors. This configuration ensured a photon flux of ~ 2 × 10 11 photons per second at the measurements conditions. The intensity of the incident beam was monitored throughout the experiments using an Ar-filled micro-ion-chamber placed between the Kirkpatrick-Baez mirrors and the HDAC. Before measurements, temperature was stabilized for about 30 min after each heating stage to ensure that chemical equilibrium was achieved inside the cell  (Louvel et al.
, 2014). In the case of coexisiting melts and fluid, careful attention was paid that measurements were performed when the melt globule was stationary and bridging both diamonds (Fig. 1F ). This configuration ensured that data collection was performed in a pure phase (either fluid or melt) without contamination of the SXRF and XAS signals by the coexisting phase to. SXRF and XAS spectra were collected in fluorescence mode in a forward scattering geometry with an energy dispersive single-element Si-detector (Ketek ® , 139 eV resolution at Mn-Kα = 5. 89 keV) set at 22° from the incident beam in the horizontal plane  (Sanchez-Valle et al. , 2003; Louvel et al. , 2013; 2014). Angle-dispersive X-ray diffraction spectra were collected on the gold pressure standard before and after XAS/SXRF measurements using a high-resolution CCD camera set in transmission geometry.