A nocturnal atmospheric loss of CH(2)I(2) in the remote marine boundary layer

Ocean emissions of inorganic and organic iodine compounds drive the biogeochemical cycle of iodine and produce reactive ozone-destroying iodine radicals that influence the oxidizing capacity of the atmosphere. Di-iodomethane (CH(2)I(2)) and chloro-iodomethane (CH(2)ICl) are the two most important organic iodine precursors in the marine boundary layer. Ship-borne measurements made during the TORERO (Tropical Ocean tRoposphere Exchange of Reactive halogens and Oxygenated VOC) field campaign in the east tropical Pacific Ocean in January/February 2012 revealed strong diurnal cycles of CH(2)I(2) and CH(2)ICl in air and of CH(2)I(2) in seawater. Both compounds are known to undergo rapid photolysis during the day, but models assume no night-time atmospheric losses. Surprisingly, the diurnal cycle of CH(2)I(2) was lower in amplitude than that of CH(2)ICl, despite its faster photolysis rate. We speculate that night-time loss of CH(2)I(2) occurs due to reaction with NO(3) radicals. Indirect results from a laboratory study under ambient atmospheric boundary layer conditions indicate a k (CH2I2+NO3) of ≤4 × 10(−13) cm(3) molecule(−1) s(−1); a previous kinetic study carried out at ≤100 Torr found k (CH2I2+NO3) of 4 × 10(−13) cm(3) molecule(−1) s(−1). Using the 1-dimensional atmospheric THAMO model driven by sea-air fluxes calculated from the seawater and air measurements (averaging 1.8 +/− 0.8 nmol m(−2) d(−1) for CH(2)I(2) and 3.7 +/− 0.8 nmol m(−2) d(−1) for CH(2)ICl), we show that the model overestimates night-time CH(2)I(2) by >60 % but reaches good agreement with the measurements when the CH(2)I(2) + NO(3) reaction is included at 2–4 × 10(−13) cm(3) molecule(−1) s(−1). We conclude that the reaction has a significant effect on CH(2)I(2) and helps reconcile observed and modeled concentrations. We recommend further direct measurements of this reaction under atmospheric conditions, including of product branching ratios.