dataesr/scientific-paragraphs-categorization huggingface dataset:
3 ± 5. 1 Ma (MSWD C+E = 1. 3) can be calculated out of three equivalent analyses. Following Chelle-Michou et al. (2017), we interpret this date as reflecting the age of partial melting in this part of the Lower Gneiss Unit. Apart from this sample, our dataset is indicative of scant zircon neo-and/or re-crystallization during Variscan metamorphism as Variscan grains are commonly lacking and overgrowth zones are scarce and narrow. Even though the investigated samples equilibrated at amphibolite-facies conditions, reaching partial melting for two of them, the Variscan imprint on the zircon budget remained very limited, and the zircon age distribution clearly records the pre-Variscan evolution of the protoliths.
argue for a West African Craton supply while Chelle-Michou et al. (2017)  retain a Saharan Metacraton provenance. In addition, none of those authors discuss the extent to which the erosion of the Cadomian magmatic arc contributed to the observed detrital zircon age distributions in the EFMC. In this section, we therefore (i) review the geological and isotopic characteristics of the Cadomian arc and address its potential implication as a proximal source for the Ediacaran EFMC sediments; and (ii) further discuss the nature of the distal source based on the newly obtained, extensive dataset. The largest and best preserved exposures of the Cadomian magmatic arc crop out in the northern Armorican Massif (France and British Channel Islands, see Ballèvre et al. (2001) ; Brown (1995) ; Chantraine et al.
Acknowledgements C. Guilbaud  made the thin sections;  J. -M. Hénot  assisted during SEM imaging; M. Ballèvre provided the file of Fig. 1;  M. Mintrone  contributed to Fig. 2;  A. Laurent , A. Vezinet,  A. Villaros ,  V. Gardien  and  G. Mahéo  participated to stimulating discussions;  C. Storey ,  U. Linnemann  and an anonymous reviewer substantially improved the manuscript; may they all be thanked.
Southeast Pacific The southeast Pacific hosts one of the largest and most persistent stratocumulus cloud decks on Earth, as shown by  Wood (2012)  using data from the combined land-ocean cloud atlas database  (Hahn and Warren, 2007). In this region, cloud cover and cloud thickness have major impacts on the net cloud radiative effect, which raises the importance of studying the heights of these clouds. Orographically induced fog at the coastal cliff ranging from Peru to northern Chile is the major source of moisture for this region  (Pinto et al. , 2006). z base and z top of the stratocumulus clouds near the coast determine the areas where fog can provide water to the environment at the coastal cliff. The cloud heights also affect the ability of the fog to be advected further inland across the cliff.
Even though the two studies make use of a similar reference database, they measure cloud heights at different times of the day. While CALIOP has an afternoon overpass, MISR has a morning overpass, when more clouds of lesser extent are present. For a more in-depth comparison and validation of the presented algorithm, more cloud height reference observations would be desirable, including observations in different climate zones and especially over ocean. Within Europe, the European Cooperation in Science and Technology (COST) activity is expected to harmonize the networks of the different weather services (e. g. ,  Haeffelin et al. , 2016; Illingworth et al. , 2018) , enabling more intercomparisons in the future. An important strength of MIBase is the geometric approach, which is applied to create the z product from MISR measurements.
Data availability. Multiple archives providing METAR data are available. The data utilized here were downloaded from the Weather Underground archive (https://www. wunderground. com/ history/airport/, last access: 4 December 2018). The MISR Level 2TC Cloud Product data were downloaded from the NASA Langley Research Center Atmospheric Science Data Center (ftp:// l5ftl01. larc. nasa. gov/MISR/MIL2TCSP. 001/, last access: 17 October 2017). ERA-Interim data were downloaded from the ECMWF data server via Web-API. The MIBase cloud base data set  (Böhm, 2019)  is freely available at the Collaborative Research Centre 1211 database at https://doi. org/10. 5880/CRC1211DB. 19. It comprises z base retrievals globally on a 0. 25 • × 0. 25 • grid for a 3-year period  (2007) (2008) (2009). Daily files include z base retrievals derived from the MISR MIL2TCSP product for about 14 respective Terra revolutions around the Earth.
Acknowledgements. The MISR Level 2TC Cloud Product data were obtained from the  NASA Langley Research Center Atmospheric Science Data Center  (Mueller et al. , 2013). We gratefully acknowledge financial support by the  Deutsche Forschungsgemeinschaft (DFG, German Research Foundation ) -project number  268236062 -SFB 1211. We thank the seven referees for their constructive feedback. Edited by: Alexander Kokhanovsky Reviewed by: seven anonymous referees.
Multivariate analyses of subfossil chironomid data A constrained sum-of-squares cluster analysis (CONISS) for percentage data was performed with R version 3. 2. 2 and the package "rioja" (Juggins 2017) to highlight major changes in chironomid assemblage composition throughout the stratigraphy  (Grimm 1987). Principal component analysis (PCA) (Fig. 3 ) was performed on a data percentage matrix of nine taxa for 16 samples. The PCA was carried out with "ade4" and "vegan" packages in R software (R Core Team 2012). Beforehand, data were square-root-transformed with the aim of stabilizing the variance. Rare taxa (present in only one sample or with a relative abundance always <5%) were excluded from analyses.
Acknowledgements We wish to thank the  Agence Nationale de Recherche (ANR)  as well as the  Centre National de la Recherche Scientifique (CNRS)  for their financial support of this study under the  Franco-German ANR/DFG  project " PALEOPERSEPOLIS==  ( ANR-14-CE35-0026-01 ) and the  Franco-Iranian International Associated Laboratory project called "HAOMA ". We also thank  Marine Leteurtrois  and  Gwenaël Magne  for their assistance in data acquisition. We wish to thank  Professors Neil Roberts  ( Plymouth University ) and  Lora Stevens  ( California State University at Long Beach ) for their helpful comments on the interpretation of our data. Finally, we extend our gratitude to two anonymous reviewers for their thoughtful and constructive comments on an earlier version of this paper.
Clay minerals were identified using their main diffraction (d 001 ) peak and by comparing the three diffractograms obtained. Estimated proportions of each clay mineral were performed using the MacDiff 4. 2. 5 software  (Petschick, 2000)  on glycolated diffractograms. As the main (d 001 ) peak of kaolinite and the (d 002 ) peak of chlorite are overlapping, a deconvolution procedure was applied on the (d 004 ) peak area of chlorite (3. 54 Å) and (d 002 ) peak area of kaolinite (3. 57 Å) to estimate properly both mineral's proportions using the 7. 1 peak (d 001kaolinite + d 002chlorite ). Chlorite percentage was calculated using the mean between (d 001 ) and (d 002 ) chlorite peak areas considering that the chemical nature in the chlorite impacts the (d 001 )/(d 002 ) ratio  (Moore & Reynolds, 1997).
ACKNOWLEDGEMENTS: This is a contribution to the  JET  project. We acknowledge funding from the  International Continental Scientific Drilling Program (ICDP)  and the  Natural Environment Research Council (NERC)  (grant number  NE/N018508/1 ). We thank the  British Geological Survey (BGS) , especially  Scott Renshaw  and  Tracey Gallagher  for facilitating access to the Mochras core over an extended period. Clemens Ullmann (Exeter),  Jim Riding  (BGS) and  Emanuela Mattioli  (Lyon) are all thanked for organizing and sharing samples. We thank  Ludovic Bruneau  and  Jeannine Lherminier  for technical assistance on XRD and TEM respectively. Dr. Branimir Segvic  and an anonymous reviewer are gratefully acknowledged for helpful comments on the manuscript.
Samples description We use the same samples studied by Di  Muro et al. (2014). These include the pre-caldera olivine-basalts (CM labels) erupted between April 2nd and 4th, and post-caldera crystal-rich oceanites (251 labels) emitted near the end of the eruption on April 25th. Oceanites contain up to 60 wt% of olivine phenocrysts ranging from mm to several cm; we have focused on crystals <2 mm. We measured the chemical zoning patterns of a subset of olivine crystals, which were previously studied for their melt inclusion composition and volatile contents  (Di Muro et al. , 2014). We also report new isotopic analyses of H (values expressed as δD VSMOW ) for some of these inclusions. Our new dataset includes the zoning patterns of 13 and 14 olivine crystals from the CM-and 251-samples, respectively, and the δD measurement in 25 melt inclusions.
Analytical methods We have used standard procedures for the data acquisition and modeling that we summarize below. Further details can be found in the Supplementary Material. The quantitative analyses and the X-ray elemental distribution maps of olivine were obtained using a JEOL JXA 8530F field emission Electron Probe MicroAnalyzer (EPMA). The crystallographic axes were determined by Electron Backscattered Diffraction (EBSD) using a JEOL JSM-7600F equipped with an Oxford/HKL detector and HKL CHANNEL5 software (both at Nanyang Technological University, Singapore). The analytical conditions are detailed in the Supplementary Material and are the same as in  Albert et al. (2015). Major, trace, and volatile (H 2 O, CO 2 , S and Cl) element concentrations in melt inclusions have been published in Di  Muro et al.
Mg-Fe, Ca, Ni and P diffusion in olivine Twenty-three rim-to-core, and eight melt inclusion-to-crystal boundary concentration profiles in olivine were obtained for Si, Fe, Mg, Ca, Ni and P (depending on the crystal). We modeled the Fe-Mg, Ni and Ca concentration gradients using the program DIPRA  (Girona and Costa, 2013). We apply the anisotropy correction to the results according to equation #5 of  Costa and Chakraborty (2004). We report the uncertainty on diffusion times that accounts for analytical and temperature uncertainty as calculated by DIPRA. In addition, DIPRA also calculates a parameter called "discrepancy", which is basically a goodness of the fit  (Girona and Costa, 2013)  and which is reported in Table  1. Most of our diffusion times were obtained from fits with a discrepancy of ≤10%.
H + diffusion The H 2 O content of the melt inclusions may vary due to postentrapment diffusion of H + through the host olivine or/and due to degassing  (Lloyd et al. , 2013; Bucholz et al. , 2013; Chen et al. , 2011; Gaetani et al. , 2012). Thus, it is critical to determine the extent to which melt inclusion data record a variation of entrapment depths versus the partial re-equilibration via dehydration during magma ascent or cooling on the earth's surface. Here we make use of the H 2 O and δD values and attempt to establish the roles of each process. We have modeled the diffusive re-equilibration of H 2 O of eight melt inclusions using the method of  Qin et al. (1992) , which considers a spherical melt inclusion of radius a hosted in a spherical crystal of radius b, and we report the details of the parameter values and equations used in the calculation in Supplementary Material.
(2016) , the two models provide very similar results in the pressure range <1 kbar typically recorded by melt inclusions in PdF oceanites. Average pressure calculated using both models corresponds to a lithostatic depth range of 1280-1100 m below the volcano summit (ca. 1. 5 km above sea level) considering a linear density increase from 1600 to 3400 kg m -3 (Di  Muro et al. , 2014). The maximum pressure recorded by the 2007 melt inclusion dataset is consistent with magma stor-  constant temperature is recorded in some melt inclusions of the post caldera phase. On the contrary, melt inclusions of the precaldera phase having experienced marked post-entrapment modification do not show significant water loss. The δD of melt inclusions varies from -135 to -10. 3h and -77 to 62h, for the pre-and post-caldera samples, respectively (Table  2 ).
The lateral transport under Piton de la Fournaise have an associated change in depth of about 1. 5 km, and this will generate a change in the magma intensive conditions (e. g. temperature and water loss). Such short times for creating olivine mushes are also consistent with the evidence of fast growth provided by the fine P skeletal zoning  (Welsch et al. , 2014; this paper). However, given the limited size of our dataset we cannot fully discard the possibility that cumulates contain some crystals recycled from previous events, as suggested by the Sr isotopic differences between the olivine separates and the bulk-rock. These older cumulates are likely represented in the crystal populations larger than those examined in this study.
Acknowledgements We thank  F. R. Fontaine  for sharing the tilt data and the OVPF for the data and sample collection. We are grateful for the discussion about surface deformation implications with  C. Lopez , and about degassing modeling with  J. De Hoog. We thank  D. Rasmussen , an anonymous reviewer, and editor  T. Mather  for their contributions that helped much to improve the manuscript. H. Albert and F. Costa were supported by a  National Research Foundation   Investigatorship Award  (grant number  NRF-NRFI2017-06 ) from Singapore.
The slab dragging is resisted by the mantle and this resistance translates into further crustal deformation at the surface  17. Such recent deformation has been documented, for example, along the Yusuf Fault System, Carboneras Fault System and especially along the AIFS and associated structures of the Rif and the Eastern Betics Shear Zone (Figs. 1  and 2b ), which comprise the main fault systems of the TASZ  19  (Figs. 1  and 2 ). Here we present a new and comprehensive geological and geophysical dataset of the entire AIFS. We adopted a multi-scale approach, including detailed morphological analysis of shipboard multibeam bathymetry and near-bottom bathymetry obtained with Autonomous Underwater Vehicles (AUVs), and interpretation of deep penetration multichannel-seismic (MCS) data (Figs. 2a  and 3 ).
3a-c ) using multibeam sonars mounted on two AUVs (see Methods). Multi-scale acoustic mapping techniques, such as swath-bathymetry allow identifying the geomorphological expression of active faults, such as seafloor ruptures, fault scarps and fault traces  27, 28. The AUV bathymetric data clearly highlight the surface expression of the AIFS, whose   3a-c ). According to the fault trend, geometry and timing of activity, the AIFS can be divided into three main segments: north, central and south. Related nearby structures, such as the NSF and the Bokkoya and Trougout faults are also considered part of the AIFS (Fig. 2b ). The NSF is a ~20-km-long, 5-km-wide left-lateral shear zone composed of a succession of closely spaced N160 trending en echelon elongated troughs (Figs. 2a  and 3a ). South of it, the North AIFS segment is 34-km-long, it trends N018 and is of Quaternary age  4, 23.
5s TWTT thick)  32. The age of deformation is derived from the seismostratigraphic interpretation combined with scientific and commercial wells available in the Alboran Basin  4, 23, 31, 33. We assume that if a given stratum displays a roughly constant thickness across the fault zone, then that stratum must have been deposited prior to the initiation of a particular fault segment. For example, in profiles TM2 and TM3 (Central AIFS segment), deformation starts in the Early Pliocene (Unit IIc-d), while in profiles TM1 (South AIFS segment) and TM28 (North AIFS segment), deformation starts post unit IIa-b (Early Pleistocene to Holocene in the Quaternary). Our interpretation fits with older data and more recently acquired MCS profiles in the Alboran Basin  4, 23, 31, 33. Hence, this allows proposing a new seismostratigraphic model  34  (Fig.
Methods Multibeam bathymetry. Multibeam shipboard bathymetry was acquired during the 2006 IEO and IMPULS, 2010 EVENT-DEEP, 2011 TOPOMED-GASSIS, 2012 SARAS and MARLBORO-2, 2015 SHAKE, and 2016 IDRISSI cruises. Hullmounted multibeam data along the AIFS were acquired with a 1 o ×1 o beam width Atlas Hydrosweep DS multibeam echosounder (R/V Sarmiento de Gamboa) and were processed with the CARIS HIPS&SIPS 9. 0 software and gridded at 20 m resolution. For the whole Alboran Sea we used the IEO 25 m multibeam compilation  60. Ultra-high-resolution, near-bottom bathymetry data were acquired with a Simrad EM2040 multibeam echosounder installed on the Autonomous Underwater Vehicles (AUVs) AsterX and IdefX from IFREMER (France) during the SHAKE cruise onboard the R/V Sarmiento de Gamboa in May 2015. The AUV surveys were conducted at ~70 m above the seafloor, in the North, Central and South AIFS segments covering areas of 43, 40 and 32 km 2 , respectively.
The AUV inertial navigation was corrected using the ultra-short baseline (USBL) acoustic navigation as a reference. The navigation of the AUV was ultimately post-processed and corrected with the CARAIBES 4. 3 software. Multibeam bathymetry was processed with the CARIS HIPS&SIPS 9. 0 software and gridded at 1 m cell size. Seismic reflection. The multichannel seismic (MCS) profiles used in this work were acquired during the 2011 TOPOMED-GASSIS cruise onboard the Spanish R/ V Sarmiento de Gamboa. During the TOPOMED-GASSIS cruise, multichannel seismic data were acquired using a 50. 15 l (3060 ci) airgun source composed by 8 G-GUN II guns deployed at 7. 5-9 m depth working at 2000 to 2500 psi, in a single and cluster distribution geometry of five gun positions: 380 × 2, 520, 250 × 2, 520 and 380 × 2 (c.
i. ). Seismic signals were acquired with a 5100-6000-m-long active section of a Sentinel Sercel streamer composed by 408 to 480 active sections (12. 5 m channel interval) at a depth of 10 m. Profiles TM1 and TM2 were fired at 2500 psi every ~30 m, while profiles TM3, TM22 and TM28 were fired at 2000 psi every ~40 m. Data were recorded at a sample rate of 2 ms and a record length of 12-14 s, except for TM28, which was recorded at a record length of 19 s. The MCS profiles were processed using Globe Claritas seismic processing software (http://www. globeclaritas. com). The processing flow was designed in order to obtain the best image in both the shallower and deeper parts of the profile  3, 34. The processing sequence included the insertion of the geometry accounting for streamer feathering; a minimum phase conversion; spherical divergence correction; predictive deconvolution in the Tau-P domain (to eliminate the bubble and short period multiple reverberations); surface consistent deconvolution; Surface Related Multiple Elimination (SRME) demultiple; normal-move-out correction based on semblance velocity analysis; Radon filter demultiple; Dip Move-Out (DMO) correction; a zero-phase conversion and a time migration.
The final image had a time and spatial variant filter to remove the incoherent noise, and an amplitude correction was applied  3, 34. Furthermore, we performed a Pre-Stack Depth Migration (PSDM) of profile TM3 with the software Echos by Paradigm (http://www. pdgm. com/ products/echos/) to obtain the real geometry of the structures in depth  34. We applied the same processing flow to the shot gathers (till the DMO correction) and obtained the depth velocity model needed for the migration through an accuracy velocity analysis based on the residual analysis, first in the time domain and second in depth. Finally, we exported the time and depth migrated sections in SEG-Y format. Teleseismic waveform inversion of the mainshock. To study the mainshock of the crisis on 25 January 2016, we retrieved data from the Incorporated Research Institutions for Seismology (IRIS) data management system (DMS) for waveform inversion.
For the rupture speed Vr we tested a range of values between 1. 5 and 4. 5 km/s and finally found that a slow rupture velocity of ~2 km/s showed a minimum variance. We tested a number of different source parameterisations (including size of the rupture area) and found that the slip pattern remained robust. This suggests a shallow slip (<15-20 km) with a slip maximum near the epicentral area and the largest slip of ~100 cm at 10 km depth, where the point source inversion located the centroid. Our inversion shows similar features to the ones obtained by Buforn et al. 13. To the south, the inversion suggested that the slip propagated very close to the seabed, perhaps nurturing surface rupture (Supplementary Fig. 3 ). Further, the slip inversion indicated that slip occurred towards the north. This feature is supported by regional waveform data from Spain, showing that the azimuthal distribution of apparent source times favours the shortest rupture for stations to the north of the rupture zone, and hence corroborates a northward rupture propagation as indicated by the slip inversion (Supplementary Fig.
We tried several existing models, and the one that produced the best data fits was the WUS (Western US) model  64  (Fig. 5 , and Supplementary Table. 1). In the Supplementary Fig. 8  we include, for every moment-tensor solution, detailed information with the number of stations used, processing parameters, modelling results and data fit. Re-location procedure of the seismic sequence. Catalogue data available on the Instituto Geográfico Nacional (IGN, Spain) website (https://www. ign. es/ign/ layout/sismo. do) were used to determine epicentral locations and focal depth for over 225 local earthquakes with M L > 3. The non-linear oct-tree search algorithm Non-LinLoc  65  was used to calculate the focal parameters  61. Travel times in the model were calculated using the finite-difference solution to the eikonal equation with a grid spacing of 2 km.
e. , relaxed). In the models, we have assumed a μ′ of 0. 4, a typical Poisson ratio of 0. 25 and a Young modulus of 8 × 10 5 bar (last two parameters compute for a shear modulus of 3. 2 × 10 5 bar). Although values of μ′ lower than 0. 4 might be appropriate on strike-slip faults  68, 69  , its variation only modestly modifies the stress distribution around a fault  41, 70. The modelling was carried out using the Coulomb 3. 4 software. The source fault is the fault plane that is displaced during the earthquake. In the ΔCFS modelling, we considered the source fault to be the one that mimics the coseismic slip determined from inversion of the teleseismic waveforms, and the rupture plane corresponding to a section of the AIFS. This section is bent and extends, from south to north between -3. 61°W/35.
75°N and -3. 78°W/35. 19°N, and bends at -3. 72°W/35. 59°N (location of the epicentre). North of the releasing bend, the source fault extends for 20 km along the Central segment and strikes 031°N. South of it, the South segment extends for 45 km and strikes 007°N. Both sections are vertical and have a rake of 5°(left-lateral strike-slip with a reverse component). To mimic the slip model presented in this work (Supplementary Fig. 3 ), the source fault was divided into 1408 sub-sources, ~1-km-wide and 1. 5km-long, each with its estimated slip. The automatic seismic moment and moment magnitude calculated by the Coulomb software gives a seismic moment (M 0 ) of 8. 79 10 18 Nm and a moment magnitude (M w ) of 6. 60. These results are slightly larger than those obtained from the seismological data.
Acknowledgements This research was supported by projects  CGL2011-30005-C02-02 ,  CTM2015-70155-R  and  Acción IDRISSI (MINECO/FEDER) , shiptime on board the  R/V Sarmiento de Gamboa  and  R/V Angeles Alvariño , EuroFleets-2 grant agreement  312762 , and access to  IFREMER AUVs AsterX and IdefX (France)  through  Ocean Facilities Exchange Group (OFEG). We also thank the  Instituto Geografico Nacional (IGN, Spain)  for providing seismological data. H. P. acknowledges the  EU   Horizon 2020 programme  under grant agreement No  H2020-MSCA-IF-2014 657769. E. d'A. acknowledges the  French programme Actions Marges , the  LabexMER  ( ANR-10-LABX-19-01 ) and the EuroFleets grant agreement  228344.