Global Atmosphere Watch

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1 World Meteorological Organization Working together in weather, climate and water Global Atmosphere Watch Geir O. Braathen Atmospheric Environment Research Division, Research Department, WMO Davis, 68.6 S Ny-Ålesund, 78.9 N Geir O. Braathen, WMO, Research Department Amundsen-Scott, 90 S

2 Some history GO 3 OS BAPMoN 1967 GRUAN Science Day, Geneva, 17 November

3 GAW observes six categories of parameters Stratospheric Ozone Greenhouse Gases CO2 CH4 N2O Reactive Gases SO2 O3 SF6 Precipitation chemistry NO3K+ ph Solar UV Radiation SO42Ca2+ CO NOx Aerosols VOC GRUAN Science Day, Geneva, 17 November 2015 NH4+ Mg2+ Cl3

4 SAGs Ozone GAW UV CAS Open Programme Area Group Secretariat IGACO-Ozone-UV EPAC Total atm. deposition Greenhouse Gases Environmental Pollution & Atmospheric Chemistry IG3IS Reactive gases GURME Scientific Steering Committee Aerosols Quality Assurance & Science Activity Centres Central Calibration Laboratories World & Regional Calibration Centres GHG N2O NOAA ESRL/GMD (USA) CH4 VOC IMK-IFU (DE) JMA (JP) Precip. chem. SUNY Albany (USA) SF6 Physical aerosol properties IFT (DE) KMA (KR) Contributing networks EMPA (CH) Total O3 Optical depth O3 3 WCC (US, CA, RU) 6 Dobson RCC (JP, AU, ZA, AR, DE, CZ) 1 Brewer RCC (ES) WORCC (CH) Sondes CO2, CH4, N2O CO, SF6, Dobson O3 Brewer total O3 Ozonesondes In situ O3 NOAA ESRL/GMD (USA) Environment Canada FZJülich (DE) NIST (USA) FZJülich (DE) GAW stations & GAWSIS Pt. Barrow BSRN TCCON In situ O3, CO, CH4 Host GAW World Reference Standards Satellites & Aircraft Ny-Ålesund Alert Pallas/Sodankylä Mace Head Trinidad Head Mauna Loa CAPMoN Jungfraujoch Puy de Dôme Zugspitze/Hohenpeißenberg Monte Cimone Mt. Waliguan Izaña Assekrem / Tamanrasset Cape Verde Mt. Kenya Samoa Pyramid Minamitorishima CARIBIC Danum Valley Bukit Koto Tabang Arembepe Cape Point Amsterdam Island Ushuaia Halley Cape Grim Lauder GAW Products Neumayer South Pole World Data Centres WOUDC Ozone & UV Environment Canada (CA) Greenhouse gases WDCGG WDCA WRDC Aerosols Radiation JMA (JP) NILU (NO) MGO (RU) GRUAN Science Day, Geneva, 17 November 2015 WDCPC WDC-RSAT SUNY Albany (USA) DLR (DE) Total atm. dep. Satellite data GHG Bulletins O3 Bulletins Assessments Global fields 4

5 SAGs Ozone GAW UV CAS Open Programme Area Group Secretariat IGACO-Ozone-UV EPAC Total atm. deposition Greenhouse Gases Environmental Pollution & Atmospheric Chemistry IG3IS Reactive gases GURME Scientific Steering Committee Aerosols Quality Assurance & Science Activity Centres Central Calibration Laboratories World & Regional Calibration Centres GHG N2O NOAA ESRL/GMD (USA) CH4 VOC IMK-IFU (DE) JMA (JP) Precip. chem. SUNY Albany (USA) SF6 Physical aerosol properties IFT (DE) KMA (KR) Contributing networks EMPA (CH) Total O3 Optical depth O3 3 WCC (US, CA, RU) 6 Dobson RCC (JP, AU, ZA, AR, DE, CZ) 1 Brewer RCC (ES) WORCC (CH) Sondes CO2, CH4, N2O CO, SF6, Dobson O3 Brewer total O3 Ozonesondes In situ O3 NOAA ESRL/GMD (USA) Environment Canada FZJülich (DE) NIST (USA) FZJülich (DE) GAW stations & GAWSIS Pt. Barrow BSRN TCCON In situ O3, CO, CH4 Host GAW World Reference Standards Satellites & Aircraft Ny-Ålesund Alert Pallas/Sodankylä Mace Head Trinidad Head Mauna Loa CAPMoN Jungfraujoch Puy de Dôme Zugspitze/Hohenpeißenberg Monte Cimone Mt. Waliguan Izaña Assekrem / Tamanrasset Cape Verde Mt. Kenya Samoa Pyramid Minamitorishima CARIBIC Danum Valley Bukit Koto Tabang Arembepe Cape Point Amsterdam Island Ushuaia Halley Cape Grim Lauder GAW Products Neumayer South Pole World Data Centres WOUDC Ozone & UV Environment Canada (CA) Greenhouse gases WDCGG WDCA WRDC Aerosols Radiation JMA (JP) NILU (NO) MGO (RU) GRUAN Science Day, Geneva, 17 November 2015 WDCPC WDC-RSAT SUNY Albany (USA) DLR (DE) Total atm. dep. Satellite data GHG Bulletins O3 Bulletins Assessments Global fields 5

6 GAW in GCOS The CO 2 and CH 4 observations in GAW were recognised as Global Baseline Observing Networks of GCOS. (2005, 2011) The ozone observing components of GAW (Dobson, Brewer and ozonesondes) were recognised as Global Baseline Observing Networks of GCOS. (2007) GCOS AOPC-XIII Doc. 25 WMO/IOC/UNEP/ICSU GLOBAL CLIMATE OBSERVING SYSTEM GCOS STEERING COMMITTEE 19th SESSION GCOS SC- XIX Doc.7.2a (01. IX.2011) GCOS-GAW Agreement recognizing the WMO/GAW Global Atmospheric CO2 and CH4 Monitoring Networks as Global Baseline Observing Networks of GCOS (Submitted by J.Butler and O. Tarasova on behalf of E.Dlugokencky, GAW Greenhouse Gas SAG chair) Summary and Purpose of Document This document presents an amendment of the 2005 agreement between GCOS and the World Meteorological Organization s Global Atmosphere Watch (WMO/GAW) Programme of the Research Department, operating under the auspices of the Commission for Atmospheric Science (CAS). The agreement specifies the terms under which the WMO/GAW Global Atmospheric CO2 & CH4 Monitoring Networks will be recognized as Global Baseline Observing Networks of GCOS. Prepared by a joint GAW/GCOS group, the amendment of the original agreement has been approved by the Scientific Advisory Group for Greenhouse Gases of WMO/GAW and by the Chair of the CAS Working Group on Environmental Pollution and Atmospheric Chemistry. It is presented to the GCOS Steering Committee for approval at its 19 th Session, following the recommendation of the GCOS/WCRP Atmospheric Observation Panel for Climate (AOPC) at its 16 th Session. ACTION PROPOSED The GCOS Steering Committee is invited to recognize the subset of the WMO/GAW Global Atmospheric CO2 & CH4 Monitoring Networks as Global Baseline Observing Networks of GCOS. Annex I: Status of WMO/GAW Global Atmospheric CO2 & CH4 Monitoring Networks in 2011 Figure 1: CO2 ground-based observations in GAW. The stations with remote sensing observations are also indicated on the map. Remote sensing sites are suited for validating satellite observations, especially when properly compared to vertical profiles. The map is adopted from the WDCGG Data Summary No. 35 available at: Detailed information about GAW stations and their measurement programme is available from the WMO/GAW Station Information System (GAWSIS) which is an on-line query and mapping facility supported by MeteoSuisse. The procedures for station activation and deactivation, data management and data products have been summarized in the original agreement between WMO/GAW and GCOS. The key GRUAN Science Day, Geneva, 17 principles November of the QA/QC implemented 2015 at the ground-based stations are described in sections programme has the demonstrated quality and 6 3. WMO/IOC/UNEP/ICSU GLOBAL CLIMATE OBSERVING SYSTEM GCOS AOPC-XIII Geneva, April 2007 GCOS AOPC-XIII Doc. no April 2007 Revised version 29 August 2007 GCOS-GAW Agreement Establishing the WMO/GAW Global Atmospheric Ozone Monitoring Networks as Global Baseline Networks of GCOS (Submitted by the Secretariat) Summary and Purpose of Document In response to Action 55 from AOPC-XII, this document presents the text of agreement between GCOS and the World Meteorological Organization s Global Atmosphere Watch (WMO/GAW) programme of the Atmospheric Research and Environment Programme (AREP) Department under the Commission for Atmospheric Science (CAS). The agreement specifies the terms under which the WMO/GAW Global Atmospheric Ozone Monitoring Network will be designated as GCOS Global Baseline Total Ozone and GCOS Global Baseline Profile Ozone Networks. It furthermore specifies terms under which selected NDACC stations at a later stage could contribute to a Reference Upper Air Network of GCOS. Prepared by a joint GAW/SHADOZ/NDACC/GCOS group, the agreement is expected to be approved by the Scientific Advisory Group for Ozone of WMO/GAW and by the Chair of the CAS Working Group on Environmental Pollution and Atmospheric Chemistry. It is presented now to AOPC-XIII for consideration. ACTION PROPOSED The meeting is invited to consider for approval the proposal that the WMO/GAW Global Atmosphere Ozone Monitoring Network be designated as baseline networks of GCOS for total and profile ozone. Furthermore, selected NDACC stations should be considered as potential future contributors to a GCOS Reference Upper Air Network. Annex I: Status of WMO/GAW/SHADOZ/NDACC Global Atmospheric Ozone Monitoring Network Annex II: Agreement between GCOS and GAW Regarding the WMO/GAW/SHADOZ Global Atmospheric Ozone Monitoring Network as a Baseline Network of GCOS and selected stations of NDACC as potential future contributors to a GCOS Reference Network. Figure 1. The 132 WMO-GAW stations measuring total ozone with Dobson and/or Brewer spectrophotometers. Figure 2. The 63 WMO-GAW + SHADOZ + NDACC stations measuring profile ozone with ECC ozonesondes. Web site at (under AREP). 4. It is generally agreed that the WMO/GAW maturity to fulfil what is required of a baseline network of GCOS. WMO/GAW already supports a Global Atm (IGACO) of Observations NDACC and operating pro GAW networ are collected through the W org) and the S gov/shadoz). uses state-ofsuch as lida Transform i spectrometer the troposphe The NDACC designed to e as high quali of measurem the time the are collected through the N to WOUDC. 5. In view of XII that invest the WMO/GA (Dobson, Bre and NDACC network for t it is propose be considere a GCOS Re related to oz the stratosph

7 Station overlap between GRUAN & GAW GRUAN Science Day, Geneva, 17 November

8 Relationships between networks GAW EARLINET SHADOZ GRUAN TCCON NDACC GRUAN Science Day, Geneva, 17 November

9 GAW Report no. 201: SOPs for ozonesondes GAW Report No. 201 Quality Assurance and Quality Control for Ozonesonde Measurements in GAW For more information, please contact: World Meteorological Organization Research Department Atmospheric Research and Environment Branch 7 bis, avenue de la Paix P.O. Box 2300 CH 1211 Geneva 2 Switzerland Tel.: +41 (0) Fax: +41 (0) AREP-MAIL@wmo.int Website: GRUAN Science Day, Geneva, 17 November

10 troposphere. In the stratosphere above 20 km altitude, the sonde types start to deviate from each other quite significantly. The precision of the SPC-6A sonde decreases with altitude to about ±(5-10)% while the observed bias changes sign with altitude from about +5% at 25 km to -8% at 35 JOSIE: Jülich OzoneSonde km. This is in contrast to the ENSCI-Z sonde type that exhibits a precision of ±(4-5)% and a rather large positive bias of about 10% up to 35 km altitude. Shortly after the JOSIE 1996 campaign the ENSCI-manufacturer recommended the use of 0.5% KI, half ph buffered sensing solution for the ENSCI-Z sonde [ENSCI-Corporation, 1996], which would lower the ozone readings by about 5% Intercomparison Experiment [Johnson et al., 2002]. Figure 4-3: JOSIE-1998: Comparison of 13 tested ENSCI-Z (A) and 13 tested SPC-6A (B) ozonesondes. Results presented as averaged (± 1 σ) relative deviations of the individual sonde readings from the UV-photometer (OPM). All sondes were prepared (including use of SST1.0) and data were processed according to Komhyr [1986]: use of (i) external pump temperature; (ii) pressure dependent background current correction (IB1, measured before exposure with ozone); (iii) pump flow correction at low pressures for SPC-6A and ENSCI-Z Komhyr.[1986] (Table 3.1), (iv) No total ozone normalization. GRUAN Science Day, Geneva, JOSIE November showed 2015 clearly that the performance characteristics of the two ECC-sonde 10

11 Improvements in the Dobson Network 12 Initial Cal.-Diff. of field Dobsons (454) to Ref. Dobson in % 8 relative Difference in % "Antarctic-Dobsons" (British Antarctic Survey) Year GRUAN Science Day, Geneva, 17 November

12 Water vapour GRUAN Science Day, Geneva, 17 November

13 Water vapour, the forgotten molecule Among all the compounds relevant for atmospheric chemistry, H 2 O(g) has been neglected The GAW Programme has the responsibility for Atmospheric Chemistry in the WMO Integrated Global Observing System (WIGOS) In the OSCAR (Observing Systems Capability Analysis and Review Tool) database, there is a line for H 2 O (intended as a chemical species relevant for atmospheric chemistry) However, this line is essentially empty We need to determine the requirements for water vapour GRUAN Science Day, Geneva, 17 November

14 Water Vapour Task Team The Scientific Steering Committee for GAW (EPAC SSC) decided to adopt water vapour as a GAW parameter. By this we mean water vapour as a chemical species relevant for atmospheric chemistry and as a greenhouse gas The SSC also decided to establish a Task Team to review the current situation (capabilities) wrt water vapour measurements and to determine the requirements for such observations GRUAN Science Day, Geneva, 17 November

15 Water vapour as a greenhouse gas The total greenhouse effect is 155 W/m 2 (Trenberth). H 2 O is responsible for about 60% of this total greenhouse effect. Water vapour does not control the Earth s temperature, but is instead controlled by the temperature. The water vapour feedback doubles the warming effect of an increase in CO 2. If we add enough CO 2 to cause an increase of 1 C in the global mean temperature, the water vapour feedback will add another 1 C. GRUAN Science Day, Geneva, 17 November

16 Cover story on WMO GHG Bulletin: Water vapour WMO GREENHOUSE GAS BULLETIN The State of Greenhouse Gases in the Atmosphere Based on Global Observations through 2014 No November 2015 ISSN surface energy (W m 2 ) 50 8 SW surface SW atmosphere 40 6 LLGHG Clouds + water vapour CO 2 (ppm) T ( C) Water vapour and carbon dioxide (CO 2 ) are the major greenhouse gases (GHGs), with CO 2 the main driver of climate change. Water vapour changes largely happen as a response to the change in CO 2. Some atmospheric gases, such as water vapour and CO 2, absorb and re-emit infrared energy from the atmosphere down to the surface. This process, the greenhouse effect, leads to a mean surface temperature that is about 33 K greater than it would be in their absence. However, it is the presence of non-condensable greenhouse gases (mainly CO 2, but also methane (CH 4 ), nitrous oxide (N 2 O) and chlorofluorocarbons (CFCs)), that serve as the forcing agents. Water vapour and clouds act as fast feedbacks. Water vapour responds rapidly to changes in temperature, through evaporation, condensation and precipitation. Observations by the Global Atmosphere Watch (GAW) Programme help to investigate this in some detail. Earth s incoming short-wave (SW) solar radiation provides approximately 340 W m 2 at the top of the atmosphere; 30% of it is reflected back to space, mostly by clouds, 20% is absorbed by the atmosphere and 50% is absorbed by the Earth s surface. At equilibrium, the incoming short-wave and outgoing long-wave (LW) energy fluxes at the top of the atmosphere are in balance. Under preindustrial conditions, the energy flux was 160 W m 2 larger at the surface than at the top of the atmosphere due to the greenhouse effect. The figure shows changes in global surface energy balance relative to pre-industrial conditions with increasing CO 2 concentration. The vertical axis on the right indicates the increase in surface temperature necessary to reach the balance between incoming (SW + LW) and outgoing (LW) radiation. The green section in the figure represents the thermal energy contributed by the long-lived, well-mixed greenhouse gases, mostly CO 2. The blue section depicts the feedback contributions by water in the atmosphere as the CO 2 concentration increases. The strong water vapour feedback means that for a scenario considering doubling of CO 2 concentration from preindustrial conditions (from about 280 to 560 ppm [1] ), water vapour and clouds globally lead to an increase in thermal energy that is about three times that of long-lived greenhouse gases (LLGHGs). (The figure is based on Lacis et al., 2013.) Executive summary The latest analysis of observations from the WMO Global Atmosphere Watch (GAW) Programme shows that the globally averaged mole fractions* 1 of carbon dioxide (CO 2 ), methane (CH 4 ) and nitrous oxide (N 2 O) reached new highs in 2014, with CO 2 at 397.7±0.1 ppm, CH 4 at 1833±1 ppb [2] and N 2 O at 327.1±0.1 ppb. These values constitute, respectively, 143%, 254% and 121% of pre-industrial (1750) levels. The * Mole fraction can be interpreted as a measure of concentration. 1 atmospheric increase of CO 2 from 2013 to 2014 was close to that averaged over the past 10 years. For both CH 4 and N 2 O the increases from 2013 to 2014 were larger than that observed from 2012 to 2013 and the mean rates over the past 10 years. The National Oceanic and Atmospheric Administration (NOAA) Annual Greenhouse Gas Index shows that from 1990 to 2014 radiative forcing by long-lived greenhouse gases (LLGHGs) increased by 36%, with CO 2 accounting for about 80% of this increase. GRUAN Science Day, Geneva, 17 November

17 Cover story on WMO GHG Bulletin: Water vapour LONG-LIVED GREENHOUSE GASES 17 Surface Temperature ( C) Surface Energy (Watts/m 2 ) Solar Energy Input Sun: 4.5B yrs ago LW UpFlux at Ground Temperature Dependent Clausius-Clapeyron Induced Feedback Contribution Runaway Danger: Climate Disaster: 453 Wm 2 Current Climate: 395 Wm 2 Ice Age: 366 Wm Wm 2 cloud Reflected by: Clouds Rayleigh Surface Snowball Earth: 235 Wm 2 CO 2 GH x 2 N xco Reflected by Earth Absorbed by Earth TOA Incident Solar Energy SW Control Knob External Forcing Global Incompatibillity to Life: 0.31 = Planetary Albedo of Eath for Curent Climate Solar Radiation Absorbed by Ground Surface Greenhouse Strength GHG Forcing water vapor GeoThrm Waste Ht Tidal H 2 O+Cloud Feedback Non Condensing Green house Gases LW Control Knob Imposed Forcing Clouds Rayleigh Surface 50 Absorbed in Atmosphere Non Solar Energy Input Energy Balance (σt 4 ) vs Temperature LW Energy to Space Wm 2 279K 262 Wm 2 261K 235 Wm 2 254K Reflected to Space by: Emitted to Space 3K Cosmic Background Pluto: T E = T surf = 44K Reference: 1xC0 2 =310ppm Effective Tempeaure (K) Lacis et al., Tellus, 2013 Fig. 13. Global energy balance analysis using global equilibrium surface temperature comparisons over an extended range of CO 2 GRUAN radiativescience forcing. At Day, the Geneva, left is the energy 17 November input scale 2015 (W m 2 ) with red arrows designating solar energy input. Heavy blue arrows represent 17 outgoing energy [reflected solar, and longwave (LW) TOA flux to space]. The temperature scale in the figure interior gives the surface

18 No November 2015 Cover story on WMO GHG Bulletin: ISSN Water vapour surface energy (W m 2 ) SW surface SW atmosphere LLGHG Clouds + water vapour T ( C) Wate the m with Wate CO 2 (ppm) respo GRUAN Science Day, Geneva, 17 November

19 Water vapour as a greenhouse gas Contributions of Stratospheric Water Vapor to Decadal Changes in the Rate of Global Warming Susan Solomon, 1 Karen H. Rosenlof, 1 Robert W. Portmann, 1 John S. Daniel, 1 Sean M. Davis, 1,2 Todd J. Sanford, 1,2 Gian-Kasper Plattner 3 Stratospheric water vapor concentrations decreased by about 10% after the year Here we show that this acted to slow the rate of increase in global surface temperature over by about 25% compared to that which would have occurred due only to carbon dioxide and other greenhouse gases. More limited data suggest that stratospheric water vapor probably increased between 1980 and 2000, which would have enhanced the decadal rate of surface warming during the 1990s by about 30% as compared to estimates neglecting this change. These findings show that stratospheric water vapor is an important driver of decadal global surface climate change. Over the past century, global average surface temperatures have warmed by about 0.75 C. Much of the warming occurred in the past half-century, over which the average decadal rate of change was about 0.13 C, largely due to anthropogenic increases in well-mixed greenhouse gases (1). However, the trend in global surface temperatures has been nearly flat since the late 1990s despite continuing increases in the forcing due to the sum of the well-mixed greenhouse gases (CO 2, CH 4, halocarbons, and N 2 O), raising questions regarding the understanding of forced climate change, its drivers, the parameters that define natural internal variability (2), and how fully GRUAN these Science terms areday, represented Geneva, in 17 climate November models further below. 19 Here we use a combination of data and models to poorly (9), and even up-to-date stratospheric chemistry-climate models do not consistently reproduce tropical tropopause minimum temperatures (10) or recently observed changes in stratospheric water vapor (11). Because of these limitations in prognostic climate model simulations, here we impose observed stratospheric water vapor changes diagnostically as a forcing for the purpose of evaluation and comparison to other climate change agents. However, in the real world, the contributions of changes in stratospheric water vapor to global climate change may be a source of unforced decadal variability, or they may be a feedback coupled to climate change, as discussed Increases in stratospheric water vapor act to RESEARCH ARTICLES Occultation Experiment (HALOE) that flew on the Upper Atmosphere Research Satellite (UARS) from late 1991 through November 2005, with coverage extending from the tropopause to the stratopause over 65 S to 65 N (16). Figure 1A shows the time series of mid-latitude water vapor in the lower stratosphere based on HALOE and balloon sonde measurements (17), along with two additional (and independent) sets of satellite data from the Stratospheric Aerosol and Gas Experiment II (SAGE II) (18) and from the Microwave Limb Sounder (MLS) (19) instruments. Taken together, these data provide strong evidence for a sharp and persistent drop of about 0.4 parts per million by volume (ppmv) after the year to Observations of lower-stratospheric tropical ozone changes also reveal a sharp change after 2000 (15). Before this decrease, the balloon data suggest a gradual mid-latitude increase in lower-stratospheric water vapor of more than 1 ppmv from about 1980 to The HALOE data as well as other Northern Hemisphere midlatitude data sets also support increases in lowerstratospheric water vapor during the 1990s of about 0.5 ppmv (15, 20). Using HALOE data, the annual average water vapor difference before and after the persistent drop at the end of 2000 is contoured in Fig. 1B. Averages were constructed on a seasonal basis for two comparison periods, from and for Only measurements above Stratospheric water vapour increased between 1980 and 2000, but decreased by about 10% from 2000 the tropopause were used; i.e., water vapor changes in the troposphere were not included in the analysis. Figure 1B shows that substantial water vapor decreases after 2000 extend throughout the bulk of the stratosphere, with the largest magnitudes in the lowermost tropical and subtropical rom on February 18, 2015 This decrease in water vapour acted to slow the rate of increase in global surface temperature by 25% over

20 Water vapour as a chemical compound Major source of HO x in clean (hydrocarbon poor) air: O 3 + hn (l<340nm) O 2 + O( 1 D) O( 1 D) + H 2 O 2OH => OH depends mainly on ozone The same process is also the dominant loss process for ozone This makes the ozone lifetime in the marine boundary layer dependent on: a. absolute concentrations of water vapour (i.e. temperature) b. overhead ozone GRUAN Science Day, Geneva, 17 November

21 The role of water in ozone depletion Without polar stratospheric clouds Ultraviolet light CI O 3 NO 2 CIO CH 4 With polar stratospheric clouds Visible light CI 2 Cl O 3 Cl O 3 Reservoirs ClO + ClO Cl 2 O 2 O 2 O 2 Visible light HNO 3 O 2 Heterogeneous chemistry on the ice particles in polar stratospheric clouds (PSC). The critical temperature for formation of Type 1 PSCs depends on the concentration of water vapour and HNO 3. More water vapour in the stratosphere will lead to more PSCs and more ozone depletion as long as there are ODSs around. GRUAN Science Day, Geneva, 17 November

22 World Meteorological Organization Working together in weather, climate and water Thank you for your attention! Geir O. Braathen, WMO, Research Department