dataesr/scientific-paragraphs-categorization huggingface dataset:
Once more, both IASI and CARIBIC display similar variations and the aircraft data stay within the monthly standard deviation (light-blue shaded area in Fig. 4 ) retrieved from IASI with the two exceptions of very high values measured locally on 12 December 2010 and 18 January 2011. These two days illustrate the high variability of mid-tropospheric methane that is particularly seen on the ocated with CARIBIC measurements. The blue envelope gives the IASI monthly deviation along the aircraft tracks. With the exception of November 2010 (one y), the full line corresponds to the first flight of the month, and the dashed line urn flight on the following day. two CARIBIC flights performed on 18 and 19 January 2011 (Fig. 4c ): between 10 • S and 5 • S, a difference of more than 60 ppbv is observed in methane between the two flights.
To compare both datasets, individual HIPPO measurements performed between 6 and 12 km (altitude range corresponding to IASI vertical sensitivity to CH 4 ) and IASI retrievals of methane are averaged in 1 • × 1 • boxes for each day of the five HIPPO missions that took place in January 2009 (HIPPO 1), October-November 2009 (HIPPO 2), May-April 2010 (HIPPO 3), June-July 2011(HIPPO 4) and August-September 2011 (HIPPO 5). The scatter plot of HIPPO CH 4 vs. IASI CH 4 for the resulting 63 collocated points is shown in Fig. 5. The comparison gives a bias of 5. 1 ppbv and a standard deviation of 16. 3 ppbv.
, 1994). Figure  6a  shows the fitted methane cycle estimated from IASI data over the IASI period (July 2007 to December 2011) for the entire tropical region. Also shown are the deseasonalized trend function and its associated standard deviation. The growth rate of methane given by the derivative of the deseasonalized trend function is plotted in Fig. 6b. An increase of methane in the mid-troposphere in the tropical region is clearly seen in this figure, with the highest increase rate in 2007-2008. Unfortunately, the beginning of the increase (end of 2006-beginning of 2007) is missed by IASI, which was declared operational in July 2007. In the following years, the rate of increase of methane appears to be decreasing, with an average increase of ∼2 ppbv yr -1 in 2009 and 2011 and of ∼5 ppbv yr -1 in 2010.
Acknowledgements. This research has received funding from the  European Union 's  Seventh Framework Programme  ( FP7/2007-2013 ) under Grant Agreements no. 218793  and  283576  (MACC and MACC-II projects) and from the  ESA GHG-CCI  project. We particularly wish to thank  Cathy Boone  and the  Ether Thematic Center team  for their help in getting IASI data, which are received through the EUMETCast near-real-time data distribution service. Thanks are due to ECMWF for making their forecasts and reanalysis available through the ECMWF data server http://www. ecmwf. int/. Calculations were performed at IDRIS, the computer centre of  CNRS, and at ClimServ , the data and computer centre of IPSL. Edited by:  A. Richter The publication of this article is financed by  CNRS-INSU.
Carbon and oxygen isotopic data The LO of Agriopleura in Western Europe was assumed to be located somewhere within the Toxancyloceras vandenheckii-Gerardhtia sartousiana zones  (Masse and Fenerci-Masse, 2008 ). This extinction is regional, that is documented from Western Europe, and is coupled with a southward migration of the genus toward the Tethyan Arabo-African margins, a pattern that was interpreted as driven by a temperature drop  (Masse and Fenerci-Masse, 2008 ). This question is here addressed by combining oxygen and carbon isotopes analyzed in sections where the LO event is identified. The carbon and oxygen isotope records (see method in appendix) were studied on bulk rock samples collected in the Mussuguet sequence near Cassis and the Agriopleura beds from Orgon, the data were used for both stratigraphic and palaeoclimatic purposes.
In addition the conjunction of these events with the magnetic anomaly M1 cannot be discounted notwithstanding the highly debated role of such perturbations in biological phenomena in general and evolutionary patterns in particular (e. g. Plotnick, 1980; Raup, 1985). The LO bioevent is therefore highly selective and shows that Agriopleura may have been a typical "tropical" form, that was more temperature dependant, than the coeval Requieniidae and Monopleuridae (see discussion in  Masse and Fenerci-Masse, 2008). This interpretation is corroborated by oxygen and carbon isotopes data gained from rudist specimens from Orgon  (Steuber et al. , 2005)  which show for a given specimen a cyclic pattern reflecting palaeoseasonality. The seasonal contrast for both oxygen and carbon values is significantly lower for Agriopleura than for the younger Requieniidae sampled after the LO event.
The construction of shallow tunnels in urban areas requires a prior assessment of their effects on the existing structures. In the case of shield tunnel boring machines (TBM), the various construction stages carried out constitute a highly three-dimensional problem of soil/structure interaction and are not easy to represent in a complete numerical simulation. Consequently, the tunnelling-induced soil movements are quite difficult to evaluate. A 3D simulation procedure, using a finite differences code, namely FLAC3D, taking into account, in an explicit manner, the main sources of movements in the soil mass is proposed in this paper. It is illustrated by the particular case of Toulouse Subway Line B for which experimental data are available and where the soil is saturated and highly overconsolidated.
NUMERICAL SIMULATION PROCEDURES The 3D procedure proposed in Fig. 5  for the simulation of the phased excavation is an attempt to accurately describe all the operations achieved by the TBM and the associated phenomena. It is implemented in the commercial numerical code FLAC3D. Using the TBM operation parameters recorded during the passage under the monitoring section (Figs. 3  and 4 ), this procedure is repeated throughout the shield progression until a stationary section is reached (stabilization of displacements),  [7]  and  [8]. The grid, 75000 nodes, is composed of eight node brick elements. The boundary con-ditions are imposed in terms of null displacements in the perpendicular direction to the faces. The extent of the grid, in the longitudinal direction, is conditioned by the position of the stationary section.
Good illustrations of this species can be found in  Takaki (1964) ,  Noguchi (1987)  and  Gao et al. (1999). Plants of Dicranum leiodontium can be confused with those of D. hamulosum Mitt. that have similarly erect and cylindrical capsules and a long-acuminate leaf apex, but the former species has a setaceous, excurrent leaf costa, while the latter has only a percurrent costa  (Noguchi, 1987). Sterile plants of D. leiodontium may be mistaken also for Dicranum klautkei Reimers, a Korean endemic identified by its somewhat curved capsule. Dicranum klautkei is known, to date, only from the type specimen collected from Kumgangsan in Onjöng-ni at Yujomsa (coll. P. Klautke 241). However, the binomial of Dicranum klautkei is misspelled as 'D. klauteri' in the TROPICOS moss database housed at MO Herbarium and also in the latest national checklist of mosses in Korea  (Ahn et al.
Acknowledgments This work was supported by The  Natural History Museum, London (BM). T. Kiebacher  is grateful to  H. Köckinger  for determining the specimen of Schistidium grande. N. G. Hodgetts would like to thank  Ron Porley  for redetermining specimens of Grimmia dissimulata from  Madeira. V. Sahu ,  A. K. Asthana  and  K. K. Rawat  are grateful to the Director,  CSIR-National Botanical Research Institute ,  Lucknow  for encouragement and providing the facilities and the  Council of Scientific and   Industrial Research, New Delhi  for financial support ( BSC-0106 ). Thanks are also due to the authorities of  GWLS ,  Forest Department ,  Uttarakhand  for providing permission and facilities to visit the area. Financial support from  SAC, ISRO, Ahmadabad, India  under project no. 3329 entitled ' Alpine ecosystem dynamics and impact of climate change in Indian Himalaya (PRACRITI-II )' is also acknowledged.
V. Dulin was performed with the financial support of Project № АААА-А16-116021010241-9: «Vegetation structural and functional organization, diversity of flora, lichen-and mycobiota of southern part of the 'Yugyd va' national park» ( 2016-2018 ) and the  Russian Foundation for Basic Research  (Projects №  15-04-03479 -а, №  16-44-110167 ). Bryophyte investigations in Asturias by  M. Infante  and  P. Heras  have benefited from the  Flora Briofítica Ibérica project (Ministerio de Ciencia y Tecnología :  Universitat Autònoma de Barcelona   2014-2016 CGL2013-40624-P ). The work of V. Fedosov was partly supported by Grant #  14-50-00029  ' Scientific basis of the national biobankdepository of the living systems' (branch 'Plants ') from  Russian Science Foundation (RNF). Y. -J. Yoon ,  S. J. Park  and  B.
No. CZ. 1. 05/2. 1. 00/03. 0100 , the  National Feasibility Programme I of the Czech Republic  Project  LO1208  and  SYNTHESYS  project  DE-TAF-4436. K. Baráth  and  P. Erzberger  thank  L. Meinunger  and  W. Schröder ,  Ludwigsstadt (Germany) , for confirming the identity of Plagiothecium latebricola. The work of  I. V. Czernyadjeva  was carried out within the framework of the institutional research project (no. 01201255616 ) of the  Komarov Botanical Institute of the Russian Academy of Sciences  and partially supported by  RFBR  (grants no. 16-04-01156 ). T. Ezer,  G. Uyar ,  M. Ören  and  M. Alatas  ¸gratefully acknowledge the financial support of the  Turkish Scientific and Technical Research Council (TUBITAK , Project Number:  114Z337 ). S. S ¸tefa ˘nut ¸acknowledges the support by project no.
Aerosol absorption properties are of high importance to assess aerosol impact on regional climate. This study presents an analysis of aerosol absorption products obtained over the Mediterranean Basin or land stations in the region from multi-year groundbased AERONET and satellite observations with a focus on the Absorbing Aerosol Optical Depth (AAOD), Single Scattering Albedo (SSA) and their spectral dependence. The AAOD and Absorption Angstr öm Exponent (AAE) data set is composed of daily averaged AERONET level 2 data from a total of 22 Mediterranean stations having long time series, mainly under the influence of urban-industrial aerosols and/or soil dust. This data set covers the 17 yr period 1996-2012 with most data being from [2003][2004][2005][2006][2007][2008][2009][2010][2011] (∼89 % of level-2 AAOD data).
Since AERONET level-2 absorption products require a high aerosol load (AOD at 440 nm > 0. 4), which is most often related to the presence of desert dust, we also consider level-1. 5 SSA data, despite their higher uncertainty, and filter out data with an Angstr öm exponent <1. 0 in order to study absorption by carbonaceous aerosols. The SSA data set includes both AERONET level-2 and satellite level-3 products. Satellite-derived SSA data considered are monthly level 3 products mapped at the regional scale for the spring and summer seasons that exhibit the largest aerosol loads. The satellite SSA dataset includes the following products: (i) Multi-angle Imaging SpectroRadiometer (MISR) over 2000-2011, (ii) Ozone Monitoring Instrument (OMI) near-UV algorithm over 2004-2010, and (iii) MODerate resolution Imaging Spectroradiometer (MODIS) Deep-Blue algorithm over 2005-2011, derived only over land in dusty conditions.
Sun-photometer observations show that values of AAOD at 440 nm vary between 0. 024 ± 0. 01 (resp. 0. 040 ± 0. 01) and 0. 050 ± 0. 01 (0. 055 ± 0. 01) for urban (dusty) sites. Analysis shows that the Mediterranean urban-industrial aerosols appear "moderately" absorbing with values of SSA close to ∼0. 94-0. 95 ± 0. 04 (at 440 nm) in most cases except over the large cities of Rome and Athens, where aerosol appears more absorbing (SSA ∼0. 89-0. 90 ± 0. 04). The aerosol Absorption Angstr öm Exponent (AAE, estimated using 440 and 870 nm) is found to be larger than 1 for most sites over 9269 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | the Mediterranean, a manifestation of mineral dust (iron) and/or brown carbon producing the observed absorption. AERONET level-2 sun-photometer data indicate the existence of a moderate East-West gradient, with higher values over the eastern basin (AAE East.
= 1. 39/AAE West. = 1. 33) due to the influence of desert dust. The North-South AAE gradient is more pronounced, especially over the western basin. Our additional analysis of AERONET level-1. 5 data also shows that organic absorbing aerosols significantly affect some Mediterranean sites. These results indicate that current climate models treating organics as nonabsorbing over the Mediterranean certainly underestimate the warming effect due to carbonaceous aerosols. A comparative analysis of the regional SSA variability has been attempted using satellite data. OMI and MODIS data show an absorbing zone (SSA ∼0. 90 at 470-500 nm) over Northeastern Africa that does not appear in the MISR retrievals. In contrast, MISR seems able to observe the East-West SSA gradient during summer, as also detected by AERONET.
We focus our study on (i) the aerosol absorption optical depth (AAOD), which is the fraction of AOD due to absorption only, (ii) the aerosol single scattering albedo (SSA), which is the ratio of aerosol scattering to total extinction (i. e. scattering + absorption), and (iii) the spectral dependence of these optical parameters, calculated in terms of Angstr öm Exponent (AE) or Absorption Angstr öm Exponent (AAE) in the case of optical depth or (1) Subsequent to the data description (ground-based and satellite remote sensing data set used in our work) in Sect. 2, the results are presented and discussed in two main parts. First (Part 3. 1-3. 2), we report AAOD and AAE AERONET level-2 and 1. 5 multiyear observations for different Mediterranean sites. In a second time (Part 3. 3), we exploit AERONET but also satellite SSA products derived at the regional scale from the Ozone Monitoring Instrument (OMI)  (Torres et al.
Aerosol level 1. 5 product As mentioned below, AERONET data quality criteria do not support the study of the brown carbon influence on absorbing properties in most cases, as smoke plumes are generally characterized by moderate AOD (0. 2 < AOD < 0. 5). However and as already mentioned, smoke aerosols that contain high concentrations of organics are characterized by large AAE (for SAFARI African biomass smoke, AAE ∼ 1. 45, calculated between 325 and 1000 nm;  Russell et al. , 2010). In order to investigate the possible role of smoke aerosols, we have conducted complementary analyses using AERONET level-1. 5 retrievals with data screened for Angstr öm Exponent > 1. 0 to avoid mineral dust aerosols. For these data (AOD > 0. 2 and AE > 1. 0), AAOD uncertainties are about 0. 01 (O. Dubovik, personal communication, 2013).
7 were derived during summer 2003 intense heat wave event. These higher values are consistent with a large agriculture waste biomass burning smoke contribution orig- inating from the region surrounding the Black Sea and transported over Crete  (Sciare et al. , 2003 (Sciare et al. , , 2008)). This influence of wood burning shows a maximum during summertime, consistent with the maxima in AAOD observed in that season over Moldova and Northern Greece, which are on the path of air masses originating from the Black Sea region and transported over the Eastern Mediterranean. Finally, over Barcelona, even if the mean value is near unity, indicating that BC aerosol is the main contributor to absorption, a large range of AAE is also observed, with maxima around 1. 6. Further analysis is needed to link the calculated AAE with the chemical composition of aerosols over different AERONET sites when such data are available.
15 or 0. 2 (at 550 nm), and in such cases, should not be used for quantitative analysis according to the MISR Data Quality Statement distributed with the aerosol products. Aerosol type information content also diminishes as AOD decreases below certain values for all remote sensing techniques (this effect is not as well documented for MODIS and OMI). Over the Mediterranean Sea, MISR derives lower SSA (∼ 0. 92-0. 96) compared to land surfaces, associated with a northsouth gradient. One can clearly note specific regions with low SSA (∼ 0. 85-0. 90) over the Aegean, Adriatic and Black Seas, possibly due to the presence of anthropogenic absorbing particles. For the spring period (Fig. 14 ), Southern Europe (Italy, Greece, Turkey and Spain) appears to be less absorbing than during summer, with ΔSSA (spring minus summer SSA) of +0.
Conclusions A multi-year climatology of column-effective aerosol absorption properties obtained over the Mediterranean from AERONET ground-based and satellite (MISR, OMI, MODIS Deep Blue) remote sensing observations is presented. The focus of this study was on characterizing Aerosol Absorption Optical Depth (AAOD) and Single Scattering Albedo (SSA), and their spectral dependence. The AAOD data set is composed of daily averaged AERONET level 2 data from 22 stations mainly under the influence of urbanindustrial and/or soil dust aerosols. The data sets span 1996-2012, but most data are from the 2003-2011 period. The SSA data set includes both AERONET and satellite products. Since AERONET level 2 absorption products are limited to high aerosol load (AOD at 440 nm > 0. 4), which are most often related to the presence of desert dust, we also considered level 1.
22 and 1. 77, respectively. The complementary analysis using level 1. 5 AERONET retrievals with data screened to avoid mineral dust aerosols (i. e. , AOD > 0. 2 and Angstr öm Exponent > 1. 0) show that some Mediterranean sites are affected by organic absorbing aerosols (mean AAE ∼ 1. 15), especially Rome, Lecce, Burjassot and Athens. The effect is found to be lower for the Barcelona and Forth Crete AERONET sites (mean AAE of about 1. 0). This result highlights that current regional climate models that treat OC as purely scattering over the Mediterranean underestimate the total warming effect of carbonaceous aerosols and neglect part of the atmospheric heating due to particles. In addition, we explored the possibility of using satellite products for characterising the spatial distribution of aerosol absorption over the Mediterranean.
Supplementary key words body mass index • glycerol • subcutaneous adipose tissue Excess body fat is a well-established risk factor for numerous complications in the overweight and obese states  ( 1 ). Adipose tissue mass is determined by its lipid turnover; i. e. , the balance between incorporation and removal of bomb testing). However, no such relationship is observed  ( 3 ). In theory, the incorporation of 14 C from the atmosphere into the lipids could be infl uenced by seasonal factors (e. g. , crops harvested and consumed by humans and animals at different times of the year). To address this methodological issue, we reanalyzed TG age data from subcutaneous adipose tissue of 91 subjects obtained from a previous study  ( 3 ). The samples were divided into two seasonal categories: the warm period (n = 24) occurring between mid-April and mid-October and the cold period (n = 67) occurring the rest of the year.
For lipolysis in cohort two ( Fig. 3  ), similar results were obtained with the three lipolytic agents; i. e. , a negative correlation between lipolysis and BMI ( Fig. 3A-C  ; r = 0. 41-0. 48; P < 0. 0001). These relationships were independent of gender or nicotine use according to ANCOVA (values not shown). In 115 subjects, we had information about weight changes in adult life. In a multiple regression analysis of isoprenaline-stimulated lipolysis versus present, highest, or lowest BMI in adult life, only the current BMI correlated (negatively) with lipolysis ( Fig. 3D  ). Similar results were obtained with noradrenaline and dibutyryl cyclic AMP (data not shown). Since lipolysis data were expressed as a ratio between stimulated and basal lipolysis, the results might be infl uenced by variations in the rate of the latter.
Glycerol in the medium (lipolysis index) was determined, and the release in the absence of a lipolytic agent (basal) or in its presence at the maximum effective concentration was assessed. There is no consensus on how to express lipolysis data, such as per weight unit of adipocytes, per number of fat cells, or as a ratio of spontaneous (basal) lipolysis. We used the latter mode of expression since it fi tted the data best. The study was approved by the Regional Ethics Board and was performed in accordance with the guidelines in the Declaration of Helsinki. Informed consent was obtained from all subjects.
Determination of triglyceride age Since the Limited Nuclear Test Bomb Treaty in 1963, 14 C levels in the atmosphere are decreasing exponentially. Due to the long isotope half-life, this is due to diffusion of 14 CO 2 out of the atmosphere ( 9 ) which is taken up into the biotope. Because we eat plants and animals, the atmosphere 14 C content is directly mirrored in the human body. In cohort one, samples of adipose tissue were subjected to lipid extraction, and the resulting sample was processed for measurements of 12 C, 13 C, and 14 C as described ( 3 ). Data were presented as the ratio of 14 C to 12 C for each sample divided by that of a well-defi ned standard sample measured in the same year and incorporating 13 C fractionation correction as described  ( 3 ). These data were used to calculate TG age and halflife as described ( 3 ) using a linear replacement model in which age distribution of lipids within an individual was exponentially distributed corresponding to a constant turnover rate per year  ( 10 ).
If important, such effect should also be observed at the fat cell level; i. e. , large fat cells should have a greater lipid age than small ones. However, this is clearly not the case since there was no correlation between TG age and fat cell volume ( Fig. 1D  ). Furthermore, in a previous study ( 3 ) TG age was the same in small and large fat cells isolated from the same fat depot in the same subject. Thus, differences in transit-time for 14 C lipid cannot explain our fi ndings in lean versus overweight subjects. Lipolysis is a major factor determining adipocyte TG turnover. In a previous study of subjects not selected for BMI, we observed an inverse relationship between adipo- notion is based on the observation that 14 C data obtained from individuals born before, during, and after nuclear bomb testing display similar TG age half-lives ( 3 ).
Since the methods to examine the lipid turnover in human fat cells have been developed quite recently, it will take some time before long-term prospective data can be generated. However, the relationship between adipose lipolysis and current (but not previous) body weight ( Fig. 3D  ) indicates that altered lipolysis is probably a consequence of increased fat mass rather than a factor preceding the development of overweight/obesity. Finally, we do not know how lipolysis and adipocyte TG turnover are infl uenced during periods of increase or decrease in body weight within the nonobese range. Our subjects reported weight stability at the time of the investigation. In conclusion, decreased TG turnover and lipolysis activation are adipose defects that are observed already in the overweight state.