dataesr/scientific-paragraphs-categorization huggingface dataset:
In contrast, the two P. tricornutum iron-responsive elements identified in  Yoshinaga et al. (2014)  are not present in the analysed non-coding regions, suggesting that a different transcription factor should be involved in modulating the LHCX2 transcriptional response to iron availability. Similarly, we could not find the two P. tricornutum motifs identified as responsive to short-term nitrogen deprivation (from 4 h to 20 h) in  Matthijs et al. (2016) , suggesting that distinct regulatory circuits may act in the short-and long-term acclimation to nitrogen deprivation. To pinpoint possible novel regulatory motifs, we also scanned the non-coding sequences of the four isoforms using the MEME Suite program  (Bailey et al. , 2009). The analysis revealed six motifs repeated at least twice in each isoform and/or shared by more than one isoform (Table  3 ; Supplementary Fig.
Acknowledgements This work was supported by  Marie-Curie ITNs CALIPSO  ( ITN 2013 GA 607607 ) and  AccliPhot  ( ITN 2012 GA 316427 ) grants and a  Gordon and Betty Moore Foundation  grant ( GBMF 4966 ) to AF, the  French ANR 'DiaDomOil '  PROGRAMME BIO-MATIERES & ENERGIES  to AF and GF, and the  Marie Curie Zukunftskolleg Incoming Fellowship  and a  Zukunftskolleg Interim Grant  to BL.
Acknowledgements This work has been carried out with the support of  RGF (Référentiel Géologique de la France) funding. Additional funding was provided by the  POTAPYR  project. VR and JC are grateful to  D. Beziat ,  M. Thibault  and  D. Guillaume  for optical and DR-X determinations of lepidocrocite and goethite. We thank  M. Calvet ,  S. Carretier  and  C. Gautheron  for fruitful discussions. We thank the two reviewers P. Lacan,  JF. Ritz  and the Associate Editor  Y. Lagabrielle  for thorough and constructive reviews that contribute to improve the manuscript. Dr H. M. Kluijver  edited the English of the manuscript.
Analytical procedure Zircons were separated from 4 kg of rocks and were subsequently processed according to standard technique (e. g. Bosch et al. , 1996) , including magnetic separation and careful hand-picking under a binocular microscope. U-Pb dating on zircon was performed by laser ablation sector field ICP-MS at Geosciences Montpellier (France). The ICP-MS (ThermoFinnigan Element XR high resolution) was coupled to a Lambda Physik CompEx 102 excimer laser generating 15 ns duration pulses of radiation at a wavelength of 193 nm. Data were acquired at low resolution (M/M= 300) in the fast electrostatic scan mode. Signals were measured in pulse counting mode using 3 points per peaks and a 20% mass window. A pre-ablation step consisting of 7 pulses was applied to clean the sample surface. The acquisition step began with 15 s of gas blank measurement followed by 45 s of laser ablation at a frequency of 4 Hz with a spot size of 26 µm and an energy density of 10 J/cm 2.
Measured isotopic ratios were monitored with reference to the G91500 zircon standard with a 206 Pb/ 238 U ratio of 0. 17917 and a 207 Pb/ 206 Pb ratio of 0. 07488 equivalent to ages of 1062 Ma and 1065 Ma, respectively  (Wiedenbeck et al. , 1995). The standard was measured four times each five unknowns in a sequence of 2 standards, 5 unknowns and 2 standards (see  Bosch et al. , 2011 for details). Analytical data are plotted and ages calculated using the IsoplotEx program  (Ludwig 2000). Analyses in Table  3  and in the Concordia plots are ±1 errors and uncertainties in ages quoted in the text are given at ±2.
Acknowledgements This project was supported by the  Algerian-French PICS cooperation program  " Architecture lithosphérique et dynamique du manteau sous le Hoggar ". We are very grateful to the civil and military authorities at Djanet and to the  "Office du Parc National du Tassili" -OPNT (now "Office National du Parc Culturel du Tassili N'ajjer" -ONPCTA)  for help during the field work. Whole-rock analyses were measured on the  Horiba-Jobin-Yvon Ultima 2 ICP-AES  at the  IUEM, Pôle de Spectrométrie Océan, Brest, France. Céline Liorzou  is thanked for her essential geochemical contribution. Microprobe analyses were performed using the Ouest Microprobe located at Brest. Jessica Langlade  is thanked for the feldspars analyses. We are very grateful to  Rob Van der Voo  for his detailed and constructive review.
Those analyses are continuing and will be reported elsewhere (G. Delaizir et al. , in prep). In the present work we obtained high energy synchrotron X-ray diffraction (HE-XRD) data for fully glassy and partially recrystallized samples along the TeO2-Bi2O3 and TeO2-Nb2O5 joins and within the Bi2O3-Nb2O5-TeO2 system. The data provide new constraints on the local structural arrangements within the matrix glasses relative to the "anti-glass" crystallization features and events observed within the system.
Experimental High energy X-ray diffraction (HE-XRD) data were obtained over a wide Q range for three series of tellurite glasses. TeO2-Bi2O3, TeO2-Nb2O5 and TeO2-Bi2O3-Nb2O5 samples were prepared from mixtures of high purity TeO2, Bi2O3 and Nb2O5 powders melted at 850°C in Pt crucibles and quenched by dipping the bottom of the crucible in water. Along the TeO2-Bi2O3 binary, glasses containing no distinguishable crystalline Bragg peaks could only be prepared very close to the TeO2 composition (98 mole% TeO2). Glass formation extended further along the TeO2-Nb2O5 binary, up to 20 mole% Nb2O5. All of the ternary compositions studied here appeared to be fully glassy. HE-XRD measurements were performed at the Advanced Photon Source (APS) at Argonne National Laboratory (USA) using the high energy beamline 6-ID-C.
Using high energy X-rays (100. 131 keV, corresponding to =0. 123822Å) allows data collection to high values of the scattering vector (Q) with minimal corrections for absorption and multiple scattering. The incident beam was collimated to 0. 25 x 0. 5 mm. Scattered XRD patterns were collected using a Perkin Elmer model 1621 detector mounted vertically on a platform that could be moved along the beam axis to select the distance between the sample and the active areas of the detector. For these measurements the detector was typically set at ~45 cm from the sample. The sample-detector distance, coordinates of the direct beam and the angles of tilt and rotation were refined by calibration against a crystalline CeO2 standard. The detector had a 41 cm 2 active area using an a-Si active surface with spatial resolution 200 µm.
The fragility indices determined for some of the most fragile liquid systems, such as ZBLAN20 and Ca-K-nitrate (176 and 210 respectively) 37 the highdensity liquid (HDL) phase of Al2O3-Y2O3 giving rise to HDA glassy polyamorphs also has a high fragility. This analysis is consistent with previous estimates of the fragility of sodium tellurite liquids 37. Our impetration of the viscosity-temperature data for the tellurite liquids is that they result in a high density amorphous (HDA) polyamorph upon quenching, with no indication of any structural or thermodynamic transition in the supercooled state that might be associated with transformation to a low-density (LDL) liquid. That behavior is different to that observed for supercooled liquids in the Al2O3-Y2O3 system  5. During annealing the Bi0.
Acknowledgements We would like to thank  Professor Alex Navrotsky  for discussion. The HEXRD work is supported by the  US DOE Argonne National Laboratory  under contract number  DE-AC02-06CH11357. We would like to sincerely thank  Prof. Kunihiko Nakashima  ( Kyushu University ) and  Prof. Noritaka Saito  ( Kyushu University ) for supporting us on the viscosity measurements PFM acknowledges support from the  EPSRC.
ACKNOWLEDGEMENTS The authors thank  V. Krasnoselskikh  for several useful comments and suggestions. We are deeply indebted to the entire MMS team that built such wonderful instruments and an outstanding program. The work of FSM and TP was supported by  NASA  grant  NNX08AO83G. JLB, RBT and BLG were supported by  NASA  Contract  NNG04EB99C  at  SwRI. The work of OVA and FSM was also supported under  JHU/APL  Contract No. 922613  ( RBSP-EFW ). AVA is grateful to the  Dmitry Zimin Dynasty Foundation  for support. The work of IYV was supported by the  Presidental  grant  МК-7757. 2016. 2.
ANALYTICAL METHOD Halite was cleaned with isopropanol to remove surface organics and air dried, and then placed under vacuum overnight to remove interstitial and intercrystalline gas. A sample consisted of several match head-sized halite pieces (2-4 mm in diameter) that were crushed incrementally to produce five to 12 successive gas bursts. Data acquisition was performed with two Pfeiffer Prisma quadrupole mass spectrometers operating in crushfast scan (CFS) peak-hopping mode  (Parry and Blamey, 2010; Blamey et al. , 2015). The instrument was calibrated using Scott Gas Mini-Mix gas mixtures (with 2% uncertainty), and verified with capillary tubes (with 1% uncertainty) filled with gas mixtures, and three in-house fluid inclusion gas standards. Amount of gas was calculated by matrix multiplication to provide quantitative results.
Volatiles are reported in mole percent, and the 3σ detection limit for gases is ~0. 3 ppm (~1 × 10 -15 mol;  Norman and Blamey, 2001). Precision and accuracy, respectively, of seven capillary tubes with encapsulated atmosphere, in relative percent, were: N 2 , 1. 43 and 0. 05; O 2 , 5. 13 and 0. 05; and Ar, 6. 86 and 4. 60. The gas results of the capillary tubes cluster close to the global atmospheric gas content (Fig. 1 ), and they clearly demonstrate the robustness of the CFS-MS method for measuring gas in artificial and natural inclusions. All results of laboratory tubes and modern (Carlsbad [New Mexico, USA], Lake Polaris [Australia]), Messinian, Cretaceous, and Neoproterozoic halite samples are presented as water-free and large gas bursts-free data (see the GSA Data Repository 1 ). Some halites produce steady gas burst trends (Carlsbad, Lake Polaris, Messinian, Neoproterozoic 1478 and 1502) that support their homogenous nature and constant environment of crystallization, whereas those with some variability (Cretaceous and remainder Neoproterozoic; Fig.
ACKNOWLEDGMENTS We thank the  Geological Survey of Australia  for permission to sample the Empress 1A and Lancer 1 cores, the  Natural Sciences and Engineering Research Council of Canada  for financial support (grant # 7961-15 ) of  U. Brand , and the  National Natural Science Foundation of China  for support of  F. Meng  and  P. Ni  (grants  41473039  and  4151101015 ). We thank  M. Lozon  ( Brock University ) for drafting and constructing the figures. We thank the editor,  Brendan Murphy , as well as three reviewers ( Steve Kesler ,  Erik Sperling , and an anonymous reviewer), for improving the manuscript into its final form.
Differential GPS measurements For all ground control points (GCPs) and ablation stake measurements, we used a Topcon DGPS unit. Occupation times were typically 1 min with 1 s sampling, and the number of visible satellites (GPS and GLONAS) was greater than 6. GCP and ablation stake locations have an intrinsic accuracy of ±0. 01 m. For surface elevation data collected along the transverse profiles (Sect. 3. 4), a shorter occupation time (∼ 10 s) was used, and these measurements have an accuracy of ±0. 05 m relative to a fixed reference point outside the glacier. Maximum uncertainty for the transverse profile measurements is ±0. 10 m for horizontal and vertical components, with the horizontal uncertainty being usually lower.
Photogrammetric measurements were used to build DEMs over the glacier tongue downstream of cross section M (Fig. 2 ). To geometrically correct the images, GCPs that included 28 large (2 × 2 m) white painted crosses and 12 easily identifiable rocks were measured with a DGPS unit (Sect. 3. 1; Fig. 2 ). Baseline lengths between the base and the rover used for GCP measurements did not exceed 2500 m. Additional tie points (36 to 60 points depending on the pair of photographs) on the overlapping images were added to improve consistency. Photogrammetric restitutions were obtained using ArcGIS and ERDAS Stereo Analyst software, and the actual geometric correction was performed with Leica LPS software. Control points used for photogrammetric restitutions had a root mean square error of 0. 06 m in XY Z.
Unmanned aerial vehicle survey A detailed survey of the glacier surface was conducted on 22-24 November 2015 using the senseFly eBee UAV. Over the course of five survey flights, a total of 582 photos were collected with the onboard Canon Ixus from an average altitude of 325 m above the glacier surface (Fig. 2 ). Prior to the survey flights, we collected DGPS measurements of 34 ground control points that consisted of (i) red fabrics with painted white squares and (ii) white crosses used also for the photogrammetry (Fig. 2 ). Twenty-four GCPs were used to process the imagery and create a DEM with Agisoft, and 10 GCPs were reserved as independent checks on the accuracy of the DEM. The original resolutions of the orthomosaic and DEM are 10 and 20 cm respectively. The images from the survey were processed using the Structure for Motion (SfM) algorithm, which is implemented in the software package Agisoft Photoscan Professional version 1.
Elevation changes over the debris-covered area Downstream of profile N, elevation changes were calculated for two periods  (2011-2014 and 2011-2015)  by differencing DEMs obtained from terrestrial photogrammetric measurements and the UAV survey. Due to terrain obstruction, thickness changes can only be calculated for 60 % of the ablation area downstream of profile N when photogrammetry data is used. Our results show a highly heterogeneous downwasting pattern of the tongue of Changri Nup Glacier (Figs. 5  and 6 ). Overall, a negative change in surface elevation is observed over the monitored area. Mean elevation changes of -0. 95 m a -1 were obtained between 2011 and 2014, and -0. 96 m a -1 between 2011 and 2015, downstream of profile www. the-cryosphere. net/10/1845/2016/ The Cryosphere, 10, 1845-1858, 2016.
Acknowledgements. This work has been supported by the  French Service d'Observation GLACIOCLIM , the  French National Research Agency (ANR)  through  ANR-09-CEP-005-01-PAPRIKA  and  ANR-13-SENV-0005-04-PRESHINE  and has been supported by a grant from  Labex OSUG@2020  (Investissements d'avenir - ANR10 LABX56 ). This study was carried out within the framework of the Ev-K2- CNR  Project in collaboration with the  Nepal Academy of Science and Technology  as foreseen by the  Memorandum of Understanding between Nepal and Italy , and thanks to contributions from the  Italian National Research Council , the  Italian Ministry of Education, University and Research  and the  Italian Ministry of Foreign Affairs. Funding for the UAV survey was generously provided by the  United Kingdom Department for International Development (DFID)  and by the  Ministry of Foreign Affairs, Government of Norway.
This project has received funding from the  European Research Council (ERC)  under the European Union's  Horizon 2020 research and innovation programme  (grant agreement No. 676819 ). EB acknowledges support from the  French Space Agency (CNES)  through the  TOSCA Top Glaciers  project. SPOT5 HRG images were obtained thanks to  ISIS-CNES  project # 510. This work was supported by public funds received in the framework of  GEOSUD, a project  ( ANR-10-EQPX-20 ) of the program " Investissements d'Avenir " managed by the  French National Research Agency. The  International Centre for Integrated Mountain Development  is funded in part by the  governments of Afghanistan, Bangladesh, Bhutan, China, India ,  Myanmar , Nepal.
1c ). Individual analyses compare favourably with other recent measurements (shown in grey, Fig. 1 ), and most notably with recent high precision measurements  (Wang et al. , 2012). For meteorites analysed in both studies (n = 7), a correlation coefficient of 0. 6 is observed, respectable considering the limited isotopic range (0. 15h) compared to analytical uncertainty (0. 03-0. 05h). This argues against any significant sample heterogeneity or bias in analytical methods, such that values reported herein can be interpreted with confidence. Although based on a smaller dataset (n = 5), pyroxene (from nakhlites) and olivine (from Chassigny) separates define an even narrower spread than the whole rocks, extending from δ 57 Fe = -0. 04 ± 0. 05h to +0. 05 ± 0. 06h. Calculated pyroxene-whole rock fractionation factors are resolvable in the Y 000593 and Lafayette nakhlites, where 57 Fe px-nak = -0.
Acknowledgements Discussions with  Hugh O'Neill  on the thermodynamic and geochemical behaviour of the elements during planetary formation and differentiation helped to clarify a number of the concepts treated in this study; P. A. S's intellectual debt to Hugh should be obvious. Many thanks to  Ghylaine Quitté ,  Alex Halliday  and  Marc Hirschmann  for helpful suggestions on earlier versions of the work. We greatly appreciate the comments of two anonymous reviewers, one in particular that urged us to think critically regarding planetary differences and diffusive processes. The even-handed and efficient editorial input of  Bernard Marty  is gratefully acknowledged. We graciously thank  K. Righter  of  NASA  for providing the MWG samples. This work was partially supported by an  Australian Postgraduate Award and ANU Vice Chancellor's Scholarship  to P.
N U M E R I C A L A P P ROA C H To implement the algorithm for solving the minimization problem, a numerical code was developed using OpenFOAM (http://www. openfoam. org). The finite volume method (e. g. Ismail-Zadeh & Tackley 2010; chapter 3) is used in this software to solve a wide spectrum of fluid dynamic models using multiprocessor computers. Particularly, it includes the codes for numerical solution of the Stokes and advection-diffusion problems with various boundary conditions and model geometries. The model domain was discretized by 1500 hexahedral finite volumes (60 and 25 volumes in the horizontal and vertical directions). The SIMPLE method  (Patankar & Spalding 1972 ; Ismail-Zadeh & Tackley 2010, chapter 6. 5. 2) was used to determine velocity and pressure at a given temperature (the relaxation parameters are chosen to be 0.
a b s t r a c t A global compilation of glacier advances and retreats for the past two millennia grouped by 17 regions (excluding Antarctica) highlights the nature of glacier fluctuations during the late Holocene. The dataset includes 275 time series of glacier fluctuations based on historical, tree ring, lake sediment, radiocarbon and terrestrial cosmogenic nuclide data. The most detailed and reliable series for individual glaciers and regional compilations are compared with summer temperature and, when available, winter precipitation reconstructions, the most important parameters for glacier mass balance. In many cases major glacier advances correlate with multi-decadal periods of decreased summer temperature. In a few cases, such as in Arctic Alaska and western Canada, some glacier advances occurred during relatively warm wet times.
Franz Josef Land Our understanding of the fluctuations of glaciers on Franz Josef Land is based on a large collection of 14 C ages (details are provided in the SM Table  1 ) constraining positions of 16 glaciers relative to 1991e1995  (Lubinski et al. , 1999). The 14 C age on in situ moss at the Glacier B margin  (Southern Hall Island)  indicates an advance at 409 BCE e CE 223. These data also indicate that the glacier was never less extensive than today over the past 2000 years. At Sonklar Glacier (Southern Hall Island) a lateral moraine is dated to CE 718e885 by a marine shell either overlain by or incorporated inside the moraine. Yuri Glacier advanced 1. 5 km beyond its 1990 margin around CE 778e1021 and receded prior to CE 1191e1285. At Cape Lagerny (Northbrook Island) the glacier was beyond the present margin until at least CE 545e671.
New Zealand Recent glacier recession in the Southern Alps of New Zealand has led to the exposure of soils and wood buried within steep lateral-moraine walls. Radiocarbon ages on organics associated with these soils afford age constraints on underlying and/or overlaying tills  (Burrows, 1973; R€ othlisberger, 1986 ; Gellatly et al. , 1988; Grove, 2004 ) (see SM Table  1 ). According to these data the most extensive advances in New Zealand occurred around 1000 and 600 years ago and in the 19th century  (Gellatly et al. , 1988). In addition,  Wardle (1973)  counted rings of trees living on moraine ridges to place minimum-limiting ages on late Holocene moraine deposition by glaciers draining the western flank of the Southern Alps. He determined that 18 Westland glaciers constructed moraines during, or prior to, the mid-to late-18th, the early-to mid-19th, and the late 19th centuries.
Acknowledgments We are grateful to our collegues  Zhu Haifeng ,  Philipp Hochreuther ,  David Loibl ,  Andrey Nazarov ,  Vladimir Myglan ,  Irina Bushueva ,  Liudmila Lazukova ,  Vladimir Mikhalenko ,  Mikhail Alexandrin ,  Elya Zozovskaya ,  L eo Martin  for their valuable help and additional material that we requested for this paper. M. Masiokas acknowledges support from  Consejo Nacional de Investigaciones Científicas y T ecnicas (CONICET)  and  Agencia Nacional de Promoci on Científica y T ecnica  (grants PICT  2007-0379  and  PICT 2010-1438. Financial support for  V. Jomelli  was provided by the  LMI GREAT ICE , the  ANR El Paso  programme no. 10-blan-68-01  and  CEPS Green Greenland project  (grant  ANR-10-CEPL-0008 ). LDEO contribution no. 8033 G. Wiles was supported by the  U. S. National Science Foundation  under grants  ATM-0902799 ,  1202218 , and  AGS-1502186.
Bulk rock geochemical analysis To complement existing data  (Abdurachman, 1998; Preece et al. , 2013; Erdmann et al. , 2016) , bulk rock geochemistry was performed by X-ray fluorescence (XRF) on two powdered samples from the 2010 eruption. Measurements were made using a Philips PW2400 X-ray spectrometer at the Regional Analytical Centre at Saint Mary's University in Halifax, Canada.
Fractures were categorized as either being in the groundmass or through phenocrysts (excluding microlites <100 μm long). In the gridded panoramas described above, large patches of cristobalite were identified by their 'fish-scale' textures  (Komorowski et al. , 2010; Horwell et al. , 2013 ) and these patches were A C C E P T E D M A N U S C R I P T ACCEPTED MANUSCRIPT used to calibrate a greyscale threshold on the entire image using the image processing software ImageJ (see Supplementary Materials; Figure  A1 ). This procedure eased identification of interstitial cristobalite as well as the more obvious vesicle-filling patches. All areas selected by the threshold filter were confirmed visually and the image was manually segmented in Adobe Illustrator. This segmented image was used to tally the total area comprised by cristobalite.
Microstructural controls on permeability Having considered the microstructure of the Types 1, 2, and 3 rocks, we revisit the dominant microstructural controls on permeability. While convenient, simple empirical power laws do not offer insight into the physics governing permeability and should, therefore, not be taken as robust predictive models. However, changes in power law trends within datasets should signal changes in the dominant microstructural controls on permeability  (Bernard et al. , 2007; Heap et al. , 2014b; Farquharson et al. , 2015). Recent work by  Heap et al. (2014b)  and  Farquharson et al. (2015)  proposes that the porosity-permeability data of andesitic rocks from Volcán de Colima are better described using two power laws, as opposed to one. To do this,  Farquharson et al.