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@ARTICLE{Witte:858151,
      author       = {Witte, Jacquelyn C. and Thompson, Anne M. and Smit, Herman
                      G.J. and Vömel, Holger and Posny, Françoise and Stübi,
                      Rene},
      title        = {{F}irst {R}eprocessing of {S}outhern {H}emisphere
                      {AD}ditional {OZ}onesondes {P}rofile {R}ecords: 3.
                      {U}ncertainty in {O}zone {P}rofile and {T}otal {C}olumn},
      journal      = {Journal of geophysical research / D Atmospheres D},
      volume       = {123},
      number       = {6},
      issn         = {2169-897X},
      address      = {Hoboken, NJ},
      publisher    = {Wiley},
      reportid     = {FZJ-2018-07058},
      pages        = {3243 - 3268},
      year         = {2018},
      abstract     = {Reprocessed ozonesonde data from eight SHADOZ (Southern
                      Hemisphere ADditional OZonesondes) sites have been used to
                      derive the first analysis of uncertainty estimates for both
                      profile and total column ozone (TCO). The ozone uncertainty
                      is a composite of the uncertainties of the individual terms
                      in the ozone partial pressure (PO3) equation, those being
                      the ozone sensor current, background current, internal pump
                      temperature, pump efficiency factors, conversion efficiency,
                      and flow rate. Overall, PO3 uncertainties (ΔPO3) are within
                      $15\%$ and peak around the tropopause (15 ± 3 km) where
                      ozone is a minimum and ΔPO3 approaches the measured signal.
                      The uncertainty in the background and sensor currents
                      dominates the overall ΔPO3 in the troposphere including the
                      tropopause region, while the uncertainties in the conversion
                      efficiency and flow rate dominate in the stratosphere.
                      Seasonally, ΔPO3 is generally a maximum in the March–May,
                      with the exception of SHADOZ sites in Asia, for which the
                      highest ΔPO3 occurs in September–February. As a first
                      approach, we calculate sonde TCO uncertainty (ΔTCO) by
                      integrating the profile ΔPO3 and adding the ozone residual
                      uncertainty, derived from the McPeters and Labow (2012,
                      doi:10.1029/2011JD017006) 1σ ozone mixing ratios. Overall,
                      ΔTCO are within ±15 Dobson units (DU), representing
                      $~5–6\%$ of the TCO. Total Ozone Mapping Spectrometer and
                      Ozone Monitoring Instrument (TOMS and OMI) satellite
                      overpasses are generally within the sonde ΔTCO. However,
                      there is a discontinuity between TOMS v8.6 (1998 to
                      September 2004) and OMI (October 2004–2016) TCO on the
                      order of 10 DU that accounts for the significant 16 DU
                      overall difference observed between sonde and TOMS. By
                      comparison, the sonde‐OMI absolute difference for the
                      eight stations is only ~4 DU.},
      cin          = {IEK-8},
      ddc          = {550},
      cid          = {I:(DE-Juel1)IEK-8-20101013},
      pnm          = {243 - Tropospheric trace substances and their
                      transformation processes (POF3-243)},
      pid          = {G:(DE-HGF)POF3-243},
      typ          = {PUB:(DE-HGF)16},
      UT           = {WOS:000430108900019},
      doi          = {10.1002/2017JD027791},
      url          = {https://juser.fz-juelich.de/record/858151},
}