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@ARTICLE{Fadnavis:908092,
      author       = {Fadnavis, Suvarna and Chavan, Prashant and Joshi, Akash and
                      Sonbawne, Sunil M. and Acharya, Asutosh and Devara,
                      Panuganti C. S. and Rap, Alexandru and Ploeger, Felix and
                      Müller, Rolf},
      title        = {{T}ropospheric warming over the northern {I}ndian {O}cean
                      caused by {S}outh {A}sian anthropogenic aerosols: possible
                      impact on the upper troposphere and lower stratosphere},
      journal      = {Atmospheric chemistry and physics},
      volume       = {22},
      number       = {11},
      issn         = {1680-7316},
      address      = {Katlenburg-Lindau},
      publisher    = {EGU},
      reportid     = {FZJ-2022-02371},
      pages        = {7179 - 7191},
      year         = {2022},
      abstract     = {Atmospheric concentrations of South Asian anthropogenic
                      aerosols and their transport play a key role in the regional
                      hydrological cycle. Here, we use the ECHAM6-HAMMOZ
                      chemistry–climate model to show the structure and
                      implications of the transport pathways of these aerosols
                      during spring (March–May). Our simulations indicate that
                      large amounts of anthropogenic aerosols are transported from
                      South Asia to the northern Indian Ocean and western Pacific.
                      These aerosols are then lifted into the upper troposphere
                      and lower stratosphere (UTLS) by the ascending branch of the
                      Hadley circulation, where they enter the westerly jet. They
                      are further transported to the Southern Hemisphere
                      (∼15–30∘ S) and downward (320–340 K) via
                      westerly ducts over the tropical Atlantic
                      (5∘ S–5∘ N, 10–40∘ W) and Pacific
                      (5∘ S–5∘ N, 95–140∘ E). The carbonaceous
                      aerosols are also transported to the Arctic, leading to
                      local heating (0.08–0.3 K per month, an increase by
                      $10 \%–60 \%).The$ presence of anthropogenic aerosols
                      causes a negative radiative forcing (RF) at the top of the
                      atmosphere (TOA) (−0.90 ± 0.089 W m−2) and
                      surface (−5.87 ± 0.31 W m−2) and atmospheric
                      warming (+4.96 ± 0.24 W m−2) over South Asia
                      (60–90∘ E, 8–23∘ N), except over the
                      Indo-Gangetic Plain (75–83∘ E, 23–30∘ N), where
                      RF at the TOA is positive (+1.27 ± 0.16 W m−2)
                      due to large concentrations of absorbing aerosols. The
                      carbonaceous aerosols lead to in-atmospheric heating along
                      the aerosol column extending from the boundary layer to the
                      upper troposphere (0.1 to 0.4 K per month, increase by
                      $4 \%–60 \%)$ and in the lower stratosphere at
                      40–90∘ N (0.02 to 0.3 K per month, increase by
                      $10 \%–60 \%).$ The increase in tropospheric heating
                      due to aerosols results in an increase in water vapor
                      concentrations, which are then transported from the northern
                      Indian Ocean–western Pacific to the UTLS over
                      45–45∘ N (increasing water vapor by
                      $1 \%–10 \%).$},
      cin          = {IEK-7},
      ddc          = {550},
      cid          = {I:(DE-Juel1)IEK-7-20101013},
      pnm          = {2112 - Climate Feedbacks (POF4-211)},
      pid          = {G:(DE-HGF)POF4-2112},
      typ          = {PUB:(DE-HGF)16},
      UT           = {WOS:000805224600001},
      doi          = {10.5194/acp-22-7179-2022},
      url          = {https://juser.fz-juelich.de/record/908092},
}