dataesr/scientific-paragraphs-categorization huggingface dataset:
Acknowledgments We congratulate our colleagues in the CERN accelerator departments for the excellent performance of the LHC and thank the technical and administrative staffs at  CERN  and at other  CMS institutes  for their contributions to the success of the CMS effort. In addition, we gratefully acknowledge the computing centers and personnel of the Worldwide LHC Computing Grid for delivering so effectively the computing infrastructure essential to our analyses. Finally, we acknowledge the enduring support for the construction and operation of the LHC and the CMS detector provided by the following funding agencies:  BMWFW  and  FWF (Austria) ;  FNRS  and  FWO (Belgium) ;  CNPq ,  CAPES ,  FAPERJ , and  FAPESP (Brazil) ;  MES (Bulgaria) ;  CERN ;  CAS, MoST , and  NSFC (China) ;  COLCIENCIAS (Colombia) ;  MSES  and  CSF (Croatia) ;  RPF (Cyprus) ;  SENESCYT (Ecuador) ;  MoER ,  ERC IUT , and  ERDF (Estonia) ;  Academy of Finland ,  MEC , and  HIP (Finland) ;  CEA  and  CNRS/IN2P3  (France);  BMBF ,  DFG , and  HGF (Germany) ;  GSRT (Greece) ;  OTKA  and  NIH (Hungary) ;  DAE  and  DST (India) ;  IPM (Iran) ;  SFI (Ireland) ;  INFN (Italy) ;  MSIP  and  NRF (Republic of Korea) ;  LAS (Lithuania) ;  MOE  and  UM (Malaysia) ;  BUAP ,  CINVESTAV ,  CONACYT ,  LNS ,  SEP , and  UASLP-FAI (Mexico) ;  MBIE (New Zealand );  PAEC (Pakistan) ;  MSHE  and  NSC (Poland) ;  FCT (Portugal) ;  JINR (Dubna) ;  MON, RosAtom ,  RAS ,  RFBR  and  RAEP (Russia) ;  MESTD (Serbia) ;  SEIDI, CPAN, PCTI  and  FEDER (Spain) ;  Swiss Funding Agencies (Switzerland) ;  MST (Taipei) ; ThEPCenter, IPST, STAR, and  NSTDA (Thailand) ;  TUBITAK  and  TAEK (Turkey) ;  NASU  and  SFFR (Ukraine) ;  STFC  ( United Kingdom );  DOE  and  NSF (USA).
Optical absorption calculation. To calculate the optical energy absorbed in the GdFeCo stack, we use a multilayer absorption calculation  14. The electric field inside the stack is obtained through the transfer matrix method. The absorption was then obtained by calculating the divergence of the Poynting vector inside the stack. The resulting absorption per layer is reported in Table  1  in the Extended Data. The absorption profile is shown in Extended Data Figure  6. The whole GdFeCo stack absorbs 35% of the incident energy. Electrical pulse absorption calculation. We determine the electrical energy absorbed in the GdFeCo section by two steps. First, we calculate the attenuation of the electrical pulse when propagating on the CPS to the GdFeCo section. We take the Fourier transform of the electrical pulse (voltage) () in time domain to get the frequency domain spectrum ().
Acknowledgements This work was supported by the  National Science Foundation Center for Energy Efficient Electronics  (sample fabrication and laser technology) and by the Director,  Office of Science, Office of Basic Energy Sciences, Materials Sciences and Engineering Division , of the  U. S. Department of Energy  under Contract No. DE-AC02-05-CH11231  within the  Nonequilibrium Magnetic Materials Program  [MSMAG] (experimental operations). We also acknowledge partial support in the early stages of this project for conceptual design and photoconducting switch development by C-SPIN: one of the six SRC STARnet Centers, sponsored by  MARCO  and  DARPA.
Cadmium and the biological cycle Cadmium (Cd) was one of the first transition metal elements for which oceanographically consistent data was obtained  (Boyle et al. , 1976; Martin et al. , 1976; Bruland et al. , 1978; Bruland, 1980). Along vertical profiles at several locations in the oceans, a striking correlation between dissolved Cd and nutrient phosphate (PO 4 ) was reported. This was surprising as until then Cd was not known to be an element with relevance for biology. Just like PO 4 , the dissolved Cd is apparently removed from surface waters leading to very low concentrations in surface waters, and enriched in deep waters due to remineralization. Obviously Cd is a nonconservative chemical element in the oceans, i. e. its distribution is not only determined by circulation and mixing of ocean waters, but also by involvement in biological and/or chemical processes.
Cadmium isotopes in seawater In 1984 Prof. Harry Elderfield suggested to the lead author (HdB) that a strong fractionation of stable isotopes of Cd in seawater might well support the first two mechanisms of a true biological function (this akin to the well-known 13 C/ 12 C biological fractionation), yet despite much effort the team was at the time not able to produce precise measurements of Cd isotopic compositions. However recently several laboratories have been able to produce accurate datasets of Cd isotopic composition for seawater collected during our expedition  (Abouchami et al. , 2011 (Abouchami et al. , , 2014;; Xue et al. , 2013)  and elsewhere  (Gault-Ringold et al. , 2012; Conway and John, 2015a,b; Xie et al. , 2017). These breakthroughs are also based on efforts to improve reference standards and analytical methods as well as laboratory intercomparisons  (Abouchami et al.
Moreover for the western South Atlantic (part of our Geotraces section GA02) we reported δ 114 Cd values that may be interpreted by either (i) sorption of Cd onto organic ligands, or (ii) an open system, steady state, fractionation model, in combination with mixing of intermediate and deep waters  (Xie et al. , 2017). The oligotrophic North East Pacific Ocean exhibits low Cd and high δ 114 Cd in surface waters, whereas the locally very strong Oxygen Minimum Zone (OMZ) in the 600-2000 m depth range was reported to affect the Cd geochemistry  (Conway and John, 2015b). These exciting new datasets have not only shed more light on the relation of Cd and δ 114 Cd with the biological cycle, but also highlight the importance of the δ 114 Cd signature of Antarctic source waters that beyond the Antarctic Ocean proper have a major imprint (AntArctic Bottom Water, AABW; AntArctic Intermediate Water, AAIW; and Subantarctic Mode Water, SAMW) on the δ 114 Cd distribution in the entire Atlantic Ocean, if not the whole world ocean.
Therefore the underlying mechanism of the biological fractionation of Cd isotopes within the Antarctic Ocean proper is of great significance for truly understanding the world ocean distributions of both Cd and δ 114 Cd. Here we express the Cd isotopic composition in seawater relative to the international NIST SRM 3108 Cd isotope standard (std): (2) = -× δ Cd {[( Cd Cd) ( Cd Cd) ] 1} This δ 114 Cd notation is the notation of the forthcoming Geotraces 2017 International Data Product, yet please be aware that one original underlying dataset  (Xue et al. , 2013)   (3) thus a simple factor 10 conversion factor. In fact the other underlying datasets  (Abouchami et al. , 2011 (Abouchami et al. , , 2014) )  were reported in ε 112/ 110 Cd that first was converted to ε 114/110 Cd and then to δ 114 Cd.
This work Here we report the first-ever observation in the oceans of correlations between previously measured and published data for the Cd isotopic composition in surface waters of the Southern Ocean  (Abouchami et al. , 2011 (Abouchami et al. , , 2014;; Xue et al. , 2013)  with here newly reported results for [CO 2 ] as well as the concentration ratio {[CO 2 ]/[HCO 3 -]} in ambient seawater. Furthermore this is illustrated by independent biological incubation experiments previously reported by  Neven et al. (2011). Whilst these experiments do not inform directly about biological fractionation of the Cd isotopic composition the results are nevertheless useful as they enable calculation of the effective uptake ratio {[CO 2 ]/ [HCO 3 -]} by the local phytoplankton communities. Finally recommendations are given for future biological incubation experiments as required for firm validation of the hypothesis of the key mechanism of biological Cd isotope fractionation that may, or may not, cause the here reported correlations of the CO 2 system with the Cd isotopic composition of surface waters.
Measurements of Cd isotopic compositions were performed by Thermal Ionization Mass Spectrometry, with methods after  Schmitt et al. (2009a,b). By subsequent calculations this yields both the total Cd concentration and the ε 112/110 Cd isotopic composition. International Cd isotope reference materials were used that confirmed the accuracy of the measurements  (Abouchami et al. , 2012). The original reported ε 112/110 Cd dataset  (Abouchami et al. , 2011 ; see also  Abouchami et al. 2014 ) has for the purpose of the current article been converted to δ 114 Cd (Table  2 ), this also for compatibility with the dataset originally in ε 114/110 Cd units of Imperial College.
Small aliquots of the filtered seawater were analyzed on shipboard for the major nutrients phosphate, silicate and nitrate. On return the samples were analyzed as described in detail by  Xue et al. (2013). Briefly upon addition of 111 Cd-113 Cd double spike, a threestage column chemistry was employed for separation and purification of the Cd. The isotopic analyses were carried out using a Nu Plasma HR MC-ICP-MS, with data being processed offline to calculate both the total Cd concentration and the ε 114/110 Cd that here is converted to δ 114 Cd (Table  2 ). Analyses of international Cd isotope reference materials showed excellent agreement with consensus values  (Abouchami et al. , 2012).
Dissolved CO 2 in surface waters Continuous surface water pCO 2 measurements are obtained by a system permanently installed aboard Polarstern. This system draws its water from the ship's sea water supply, where sensors also continuously measure salinity S and temperature T. A steady flow of this water is led through an 'equilibrator' vessel, filling it almost halfway before flowing out of it into the ship's drain. The air in the headspace of this equilibrator takes on the pCO 2 value of the seawater. The air of this headspace is circulated through a LiCor 7000 infrared gas analyzer. Sensors data for vapour, pressure and temperature was used for regular minor corrections. Four calibration gasses (pCO 2 at 0, 175, 350 and 700 μatm) are available for hourly recalibration of the gas analyzer. Atmospheric air is measured every hour.
e. Si that is essential for the important group of diatoms, and Cd that has or can have a function in carbonic anhydrase, see main text. Each element symbol preceded by its atomic number. Major dissolved inorganic species, i. e. here not taking into account the strong organic complexation for several trace elements as discussed for Cd and Zn in the main text. Given concentrations are typical values, real concentrations vary around these as function of depth and geographic location. Please notice that the Antarctic Ocean has HNLC conditions not only for N, Si and P but also for Co, Ni, Cu, Zn and Cd, see main text. Data sources are as follows: DIC Atlantic is at Bermuda Atlantic Time Series Station (BATS) of GEOTRACES cruise GA02-64PE321 aboard RV Pelagia, station 21 (31°45. 92′N, 64°04. 95′W at 13 June 2010) after  Rijkenberg et al.
1 1. 2-1. 5 1. 6-1. 9 ~2. 3 < 0. 1 2. 5-3. 3 25 Mn Mn 2 + [nmol•kg -1 ] 0. 2-3. 0 0. 1-0. 15 0. 04-0. 5 ~0. 1 ~1-2 ~0. 2 26 Fe Fe(OH) 2 + [nmol•kg -1 ] 0. 2-2. 0 0. 6 0. 02-0. 1 ~0. 4 ~0. 05 ~0. 6 27 Co Co 2 + [pmol•kg -1 ] 3 0 6 0 2 0 -85 ~60 10-50 50-250 28 Ni Ni 2 + [nmol•kg -1 ] 2 4 5. 5-6. 5 5. 5-7. 0 2. 1 11 29 Cu CuCO 3 [nmol•kg -1 ] 0. 5-1. 5 1. 3-2. 2 1-2 2 -4 < 0. 5 5 30 Zn Zn 2 + [nmol•kg -1 ] 0. 1 2 2. 5-3. 1 6. 2-7. 8 0. 07 9 48 Cd CdCl 2 [nmol•kg -1 ] 0. 01 0. 3 0. 1-0. 6 0. 7-0. 8 0. 002 0. 8-1. 1 Table 2 Dataset for Section 4. 1. (Figs. 5 and 6 and Eqs. (  9 ) and (  10 )) and Section 4. 3. (Figs. 8, 9 and Eqs. (  12 ) and (  13 )). Also for Section 5. 6 and its Certified Reference Material (CRM, see  Dickson, 2001 ) was analyzed at least three times per day. Measurements of dissolved nutrients (silicate, nitrate and phosphate) were performed colorimetrically and on board with an auto-analyzer.
Dissolved CO 2 and Cd isotopes The δ 114 Cd values of surface waters along the Zero Meridian transect are shown in Fig. 4a. Notice here the agreement for the data of two laboratories, obtained using very different analytical methods. This confirms the overall accuracy of the datasets of both laboratories. The underway dissolved [CO 2 ] in surface waters is shown in Fig. 4b  for all data, and in Fig. 4c  for selected data only at the same station positions as the Cd isotope samples. When now plotting the δ 114 Cd as function of the dissolved [CO 2 ] a striking inverse correlation is found (Fig. 5 ) with linear regression: (9) When [CO 2 ] becomes lower the δ 114 Cd becomes higher, i. e. the ratio 114 / 110 Cd is higher. This may be explained by considering that at lower available [CO 2 ] the phytoplankton cells need to take up relatively more [HCO 3 -] to sustain growth, and this requires more carbonic anhydrase to convert the [HCO 3 -] to CO 2 suitable for use by RuBisco.
Nevertheless a best-fit line can be drawn through these 3 outliers, and this indicates an about 83-fold enhancement of the uptake ratio versus Table  3  Dataset for Section 4. 2 (Fig. 7  and Eq. (  11 )). Station CO 2 uptake % Neven Table  3  HCO 3 -uptake % Neven Table  3  eCA uptake % Neven Table  3  Sum uptake HCO the ambient seawater ratio (Fig. 7 ). In addition, notice that the cluster of stations  104, 125, 150, 167, 178, 198 together with outliers 161, 191, 216  provide similar results with fairly low uptake ratio {[CO 2 ]/ [HCO 3 -]} < 1. 0 as compared to higher uptake ratios: 2. 0 < {[CO 2 ]/[HCO 3 - ]} < 6. 0 seen for the cluster of stations  113, 186, 193, 204. Anyway at all 13 stations the uptake ratio is always higher than the ambient seawater ratio. The high value 2327. 7 found for the slope of the regression line (Eq.
Interactions with major nutrients The general upwelling of deep waters that are relatively rich in most (but not all) of the 9 bio-essential chemical elements (Eq. (  1 )) supports summer blooms of phytoplankton that partially remove the same 9 elements from the surface waters. For the major nutrients (N, P, Si) in the Antarctic Ocean there remains an ample surplus throughout the year. There also remains a high background concentration of DIC but the [CO 2 ] component decreases significantly during blooms. The other extreme of the 9 bio-essential elements is Fe as this is seriously depleted and thus limits phytoplankton growth. Given the interaction of Cd with the biological cycle, one may also look for relations of δ 114 Cd with the major nutrients in surface waters. For the same δ 114 Cd dataset these relationships are listed in Table  4 , on the basis of regression plots.
dataproduct includes the chemical profile data collected during ANT-XXIV/3), from all Alkalinity data available in the geospatial domain [65°W-5°E, 70°S-35°S; depth < 50 m]. The uncertainty of A T synth (i. e. , ± 8. 9 μmol/kg) translates to only a minor error in calculated [HCO 3 -] of ± 4. 3 μmol/kg. Comparison for the top-of-profile samples of A T synth to measured Alkalinityshows good agreement. For consistency of the 26 underway samples with the 11 bottle samples, subsequent calculations are performed using A T s ynth for all 37 samples. From the combined dataset of pCO 2 , A T synth , T, S, silicate and phosphate, the [HCO 3 -] ion was calculated using CO2SYS for Matlab(van Heuven et al. , 2011b).
Acknowledgements This article is dedicated by all authors in great appreciation to  Prof. Frank Millero , who served the community for 25 years with great enthusiasm as the editor-in-chief of  Marine Chemistry. During the same 25 years the lead author (HdB) had the great privilege to collaborate with Frank in the team of associate editors. Moreover, in earlier contacts at  Gordon Conferences  and other meetings in the 1980′s, Frank has always been very interested and keen to discuss the science with  HdB. During  and beyond the 1988 cruise in the Black Sea there was fine collaboration leading to 2 co-authored articles on the chemistry of the Rare Earth Elements in anoxic basins in context of the thesis research of  Johan Schijf  (Schijf et al. , 1994(Schijf et al. , , 1995)). This was followed in 2005 by joint authorship, with several others, of the synthesis article on in situ Fe fertilization experiments (de Baar et al.
, 2005). The lead author (HdB) sincerely recognizes the forward vision of the late  Prof. Harry Elderfield  for, some 30 years ago, sharing his keen interest in Cd isotopes in the oceans. The authors are most grateful to the late  Prof. Eberhard Fahrbach  for his excellent leadership of the Polarstern ANT XXIV/3 expedition in 2008, which was perhaps the most challenging expedition ever for each individual member of the shipboard party. Many thanks are also to  Master Stefan Schwarze  and his dedicated officers and crew for the excellent support throughout. This research is part of the  international Geotraces program  (www. geotraces. org)and was supported by the  Alfred Wegener Institute for Polar and Marine Research  for participation in the  ANT XXIV/3 expedition and sampling program. Major support was provided by research grants " International Polar Year (IPY) Geotraces " ( 851.
40. 002 ), " Dissolved Fe, Al and Mn in polar oceans " ( 851. 40. 101 ), "Observation facility of the Oceans in a High-CO 2 World ( 834. 05. 005 )," " Southern Ocean Primary Productivity in a High-CO 2 World " ( 851. 20. 031 ) from the  Netherlands Antarctic Program of the Netherlands Organization for Scientific Research (NWO) ; from a  Max Planck Society Research fellowship  to WA; and from the  UK   NERC  grant  NE/G008973/1  to MR. HdB organized the Geotraces component and several research grants for the expedition, was involved in shipboard sampling, and wrote the article with involvement and contributions by all authors. SvH did the shipboard sampling and measurements of the CO 2 system and afterwards the further CO 2 -System calculations to determine [CO 2 ] and [HCO 3 -]. JvO did the shipboard measurements of the major nutrients.
Event and track selection The data samples analyzed in this article were recorded by ALICE during the 2010 Pb-Pb and 2013 p-Pb runs of the LHC at centre-of-mass energies of √ s NN = 2. 76 TeV and √ s NN = 5. 02 TeV, respectively. The Pb-Pb run had equal beam energies, while the p-Pb run had beam energies of 4 TeV for protons and 1. 58 TeV per nucleon for lead nuclei, which resulted in a rapidity shift of -0. 465 of the centreof-mass system with respect to the ALICE laboratory system. In the following, all kinematic variables are reported in the laboratory system. Minimum bias Pb-Pb and p-Pb events were triggered by the coincidence of signals in both V0 detectors. The trigger efficiency is 99. 7% for non-diffractive Pb-Pb collisions  [54]  and 99. 2% for non-single-diffractive p-Pb collisions  [55].
The dataset of p-Pb collisions is divided into several multiplicity classes defined as fractions of the analysed event sample, based on the charge deposition in the V0-A detector. These multiplicity classes are denoted as "0-20%", "20-40%", "40-60%", and "60-100%", from the highest to the lowest multiplicity. About 13 million Pb-Pb and 92 million p-Pb minimum bias events passed all event selection criteria. This analysis used tracks that were reconstructed based on the combined information from the TPC and ITS detectors. Primary charged tracks were required to have a distance of closest approach to the primary vertex in the longitudinal (z) direction and transverse (xy) plane smaller than 3. 2 cm and 2. 4 cm, respectively. Tracks with 0. 2 < p T < 5. 0 GeV/c were selected in the pseudorapidity range |η| < 0.
Hydrodynamic calculations from VISH2+1, especially the one with MC-KLN initial conditions, overestimate the possible p T -dependent V 3 flow vector fluctuations, despite the good description for the second harmonic. A good agreement between data and hydrodynamic calculations from iEBE-VISHNU is found for all centrality intervals. This is expected for AMPT initial conditions as the calculations quantitatively reproduce both measured v 3 {2} and v 3  [2]  as discussed above. However, the calculations with Trento initial conditions, which overestimate both v 3 {2} and v 3  [2] , are consistent with the measured v 3 {2, |∆η| > 0. 8}/v 3 [2, |∆η| > 0. 8] ratio. This accidental agreement needs further investigations in the iEBE-VISHNU framework to understand the physics mechanism responsible for this behaviour.
g. shear viscosity over entropy density ratio η/s of the QGP, complementing the previous anisotropic flow measurements. The results therefore bring new insights into the properties of the QGP produced in relativistic heavy ion collisions at the CERN Large Hadron Collider. Similar studies were performed in various multiplicity classes in p-Pb collisions. Deviations of v 2 {2}/v 2  [2]  and r 2 from unity are observed, although with relatively large statistical fluctuations. For the highest p-Pb multiplicity class, the deviations are significantly overestimated by DPMJET; however, they are compatible with hydrodynamic calculations using modified MC-Glauber initial conditions and η/s = 0. 08. Meanwhile for low multiplicity p-Pb collisions, the data sits between calculations from DPM-JET and hydrodynamics.
A systemic review of the literature was performed using the Medline database. The search was performed using the terms " oral hygiene" or "periodontal" or "periodontitis" or "gingivitis" and "gastrointestinal", "esophagus", "stomach", "liver", "intestine", "intestines", "inflammatory bowel disease", "bowel", "colon", "gall bladder", "gallstone", "pancreas". A total of 708 articles were identified. After reviewing the titles and abstracts, 674 studies were excluded. A total of 34 articles were included in this literature review.
In order to conduct further studies for validating EVs as biomarkers in CVDs, large randomized clinical trials with carefully selected control groups are needed  [165]. Currently, a number of clinical trials are ongoing. The human beta cell-released EVs in the blood circulation may trigger the immune responses in the early stage of type 1 diabetes (NCT03106246). Ticagrelor was supposed to reduce the release of platelet EVs in patients with acute MI (NCT02931045). These clinical trials may push forward the applications of EVs in clinical monitoring of diseases as well as their use as biomarkers in CVDs. Meanwhile, clinical applications require efficient detection protocols and methods for circulating EVs and their components, which may depend on the progression of novel technology. In general, to establish EVs as biomarkers in CVDs, convincing clinical trials as well as efficient and standardized detection methods are prerequisites.
The fusion reaction mechanism has been widely studied in the past  [4] [5] [6] , and despite considerable efforts in both experimental and theoretical studies questions concerning the behaviour of such reactions at very low colliding energies remain open. Indeed, it can be seen in figure 1 that data show discrepancies among the various ex-⋆ e-mail: guillaume. fruet@iphc. cnrs. fr periments with large uncertainties at the lowest measured energies. Moreover, extrapolations towards the astrophysical region differ by orders of magnitude  [7]. The measurement technique will be presented in Sect. 2. The dedicated STELLA setup as well as technical developments will then be presented in Sect. 3. Fi-nally, preliminary results from the commissioning phase of STELLA will be discussed in Sect. 4.