The two principal sources of CO to the atmosphere are oxidation of CH4 and combustion. Mean rate constants for oxidation of CH4 and CO by OH in the troposphere are k 1 = 2.5x10 -15 cm 3 molecule -1 s -1 and k 2 = 1.5x10 -13 cm 3 molecule -1 s -1 , respectively. Observations indicate mean CO concentrations of 80 ppbv in the northern hemisphere and 50 ppbv in the southern hemisphere, and a globally uniform CH4 concentration of 1700 ppbv. Calculate the fraction of the CO source in each hemisphere contributed by oxidation of CH4. Comment on the interhemispheric difference.
1. Ozone is supplied to the troposphere by transport from the stratosphere. We estimate here the magnitude of this source by using the two-box model for stratosphere-troposphere exchange introduced in problem 3. 3 , where kST = 0.7 yr-1 is the transfer rate constant of air from the stratosphere to the troposphere and kTS = 0.14 yr-1 is the reverse transfer rate constant from the troposphere to the stratosphere. Observations indicate that the atmosphere contains 5x1013 moles of O3 and that 90% of that total is in the stratosphere (the remaining 10% is in the troposphere). Calculate the net source of tropospheric O3 contributed by transport from the stratosphere.
2. Ozone is also produced within the troposphere by oxidation of CO and hydrocarbons (principally CH4) in the presence of NOx. One of the earliest estimates of the global source of ozone in the troposphere was done by scaling the emission inventories of CH4 and CO. We repeat this calculation here. Consider the following mechanism for oxidation of CH4 and CO to CO2 under high-NOx conditions:
2.1 Write a net reaction for the oxidation of CO to CO2 by the above mechanism. Do the same for the oxidation of CH4 to CO2 (some of the reactions may proceed more than once). How many O3 molecules are produced per molecule of CO oxidized? per molecule of CH4 oxidized?
2.2 Present-day global emission estimates are 3x1013 moles yr-1 for CH4 and 4x1013 moles yr-1 for CO. Using your results from question 2.1, estimate the global production rate of ozone in the troposphere.
2.3 The range of estimates for the global chemical production rate of ozone in the troposphere, as derived from 3-dimensional models of tropospheric chemistry, is 6-10x1013 moles yr-1. Explain how the approach you used in question 2.2 might be expected to overestimate the production rate of ozone.
Assume the following branching ratios: (2:1) for loss of CH3O2 by (2a:2b), (1:1:1) for loss of CH3OOH by (3a:3b:3c), (2:1:1) for loss of CH2O by (4a:4b:4c). These ratios are typical of lower tropospheric air in the tropics.
1.4. What is the net number of HOx molecules consumed in the oxidation of one molecule of methane to CO 2 ? Could modifications in the branching ratios of (2), (3), (4) turn the oxidation of methane into a net source of HOx? How so? How would it be possible to modify the branching ratios?
2.2. Taking into account this recycling, how many OH molecules are actually lost in the oxidation of one molecule of methane to CO 2 ? How many OH molecules are actually lost in the oxidation of one molecule of CO to CO 2 ?
2.3. The global average CH 4 and CO emission fluxes are estimated to be 1.2 and 1.9x10 11 molecules cm -2 s -1 , respectively. Assume a fixed global average OH source from O3 photolysis of 2.9x10 11 molecules cm -2 s -1 in the troposphere , and fixed branching ratios taken from above for all reactions in the mechanism. Based on the mechanism, would OH be titrated if CH 4 emissions doubled? If CO emissions doubled?
2.4. In fact the branching ratios would change if OH concentrations changed. How could these changes help in providing stability to OH? Which branching ratio is most critical for ensuring OH stability?
1. The main sink for CH2O in the Arctic is photolysis, with a mean rate constant k = 1x10 -5 s -1 . Oxidation of CH4 is the only significant source of CH2O. Show that the steady-state concentration of CH2O is given by
2.3. One possible explanation for the difference in OH concentrations between glacial and pre-industrial times is that stratospheric ozone concentrations were higher in glacial times. Why would that be? How would that affect OH concentrations?
Recent measurements have revealed the ubiquitous presence of high concentrations of acetone in the upper troposphere, raising interest in the possible implications for tropospheric O3. Acetone is emitted to the atmosphere by both biogenic and anthropogenic sources, and is removed from the atmosphere mainly by photolysis (l < 360 nm). Consider the following mechanism for complete oxidation of acetone to CO2 in the atmosphere:
1. How many O3 molecules and how many HOx molecules are produced in the complete oxidation of one molecule of acetone to CO2 by reactions (1)-(7)? (note that some of the reactions may proceed more than once)
with rate constants k8 = 1.0x10-5 s-1, k9 = 3.6x10-11 cm-3 molecule-1 s-1, k10 = 2.2x10-10 cm-3 molecule-1 s-1. For typical conditions at 10 km altitude with 67 ppmv H2O, 50 ppbv O3, 0.5 ppbv acetone, and an air density [M] = 8x1018 molecules cm-3, compare the source of HOx from reaction (10) to that from conversion of acetone to CO2 .
3. You should have found in question 2 that photolysis of acetone is an important source of HOx in the upper troposphere. One finds by contrast that it is a negligible source of HOx in the lower troposphere or in the stratosphere. Why?
4.2. Compare the O3 production rates resulting from the oxidation of CO and from the photolysis of acetone. Do you conclude that O3 production in the upper troposphere is insensitive to changes in the concentration of acetone? Briefly explain.
We consider a simple dynamical model for the upper troposphere over the tropical oceans where direct transfer from the lower troposphere to the upper troposphere by deep convective clouds is balanced by large-scale subsidence. Let kij represent the first-order rate constant for transfer of air from layer i to layer j.
1. We estimate the residence time of air in the upper troposphere in this model by using methyl iodide (CH3I) as a tracer of transport. Methyl iodide is emitted from the oceans and has a lifetime of 4 days against photolysis. Mean CH3I concentrations are 0.36 pptv in the lower troposphere and 0.10 pptv in the upper troposphere. Assuming steady state for CH3I in the upper troposphere, show that the residence time of air in the upper troposphere is 10 days.
2. Deep convection provides a means for rapid transport of gases from the lower to the upper troposphere, but water-soluble gases are scavenged during transport by precipitation in the deep convective cloud. Consider a gas X with Henry's law constant KX (M atm-1) in a cloud of liquid water content L (volume of liquid water per volume of air). Show that the dimensionless fractionation f of X between the cloudwater (aq) and the gas phase (g) is given by
3. Calculate f for the peroxides H2O2 (KH2O2 = 2x105 M atm-1) and CH3OOH (KCH3OOH = 3x103 M atm-1) for a typical cloud liquid water content L = 1x10-6 m3 water/m3 air and temperature T = 250 K (be careful with units!). Your results should show that H2O2 but not CH3OOH is efficiently scavenged in deep convection.
4. Observed mean concentrations of CH3OOH are 1100 pptv in the lower troposphere and 80 pptv in the upper troposphere. Calculate the net source of CH3OOH (molecules cm-3 s-1) to the upper troposphere associated with deep convection. Use an air density na = 4x1018 molecules cm-3 for the upper troposphere.
Branching ratios are (1:1) for (1a:1b) and (1:1:1) for (2a:2b:2c). Calculate the yield of HOx per molecule of CH3OOH injected to the upper troposphere, and from there the total HOx source in the upper troposphere resulting from deep convective injection of CH3OOH. Compare to a typical HOx source of 1x104 molecules cm-3 s-1 in the upper troposphere from the O(1D)+H2O reaction. Is convective injection of CH3OOH an important source of HOx in the upper troposphere?
[To know more: Prather, M.J., and D.J. Jacob, A persistent imbalance in HOx and NOx photochemistry of the upper troposphere driven by deep tropical convection, Geophys. Res. Lett., 24, 3189-3192, 1997.]
Events of rapid O3 depletion are observed in arctic surface air in spring, with concentrations dropping from 40 ppbv (normal) to less than 5 ppbv in just a few days. These O3 depletion events are associated with elevated bromine which appears to originate from the volatilization of sea salt bromide deposited on the ice pack. In this problem we examine the mechanism for Br-catalyzed O3 loss thought to operate in arctic surface air. Consider a surface air parcel in the arctic at the onset of an O3 depletion event. The air parcel contains 40 ppbv O 3 , 50 pptv Bry (sum of Br, BrO, HOBr, and HBr), 10 pptv CH 2 O, 3x107 molecules cm-3 HO2, and 1x10 5 molecules cm -3 OH. The air density in the parcel is 3x10 19 molecules cm -3 . Bromine chemistry is described by the reactions:
with rate constants k 1 = 6x10 -13 cm 3 molecule -1 s -1 , k 2 = 1x10 -2 s -1 , k 3 = 3x10 -12 cm 3 molecule -1 s -1 , k 4 = 6x10 -13 cm 3 molecule -1 s -1 , k 5 = 5x10 -12 cm 3 molecule -1 s -1 , k 6 = 1.1x10 -11 cm 3 molecule -1 s -1 , and k 7 = 1x10 -4 s -1 .
3. Write an equation for the O3 loss rate (-d[O 3 ]/dt) in the catalytic mechanism as a function of [BrO]. What would the O3 loss rate be if BrO were the main contributor to total bromine (that is, if [BrO] ª 50 ppt)? Would you predict near-total ozone depletion in a few days?
4.2 Assuming steady-state for all bromine species, calculate the concentrations of HOBr, HBr, BrO, and Br in the air parcel. How does the resulting O3 loss rate compare to the value you computed in question 3? Would you still predict near-total O3 depletion in a few days?
Reaction (3) is viewed as an equilibrium process with constant K 3 = [N 2 O 5 ]/([NO 3 ][NO 2 ]) = 3.6x10 -10 cm 3 molecule -1 . Other reactions have rate constants k1 = 3x10-14 cm3 molecule-1 s-1, k 2 = 2x10 -17 cm 3 molecule -1 s -1, and k 4 = 3x10 -4 s -1 . Consider an air parcel with a temperature of 280 K, pressure of 900 hPa, and constant concentrations of 40 ppbv O 3 and 0.1 ppbv NO x .
4. Assuming that NO 3* is in chemical steady state at night (your answer to question 3 should justify this assumption), and that the night lasts 12 hours, calculate the 24-hour average lifetime of NO x against oxidation to HNO 3 by the above mechanism. Compare to the typical 1-day lifetime of NOx against oxidation by OH.
with k 1 = 2.2x10 -12 exp(-1430/T) cm 3 molecule -1 s -1 , and k 2 = 1x10 -2 s -1 (noon). How does the [NO 2 ]/[NO x ] ratio vary with time of day? How would it be affected by the presence of peroxy radicals?
2. Photolysis of acetone (CH 3 C(O)CH 3 ) is an important source of PAN. In a high-NO x atmosphere, the peroxyacetyl radical (CH 3 C(O)OO) produced by photolysis of acetone reacts with either NO or NO 2 :
3. Consider an air parcel ventilated from a city at time t = 0 and subsequently transported for 10 days without exchanging air with its surroundings. We wish to examine the fate of NO x as the air parcel ages. The air parcel contains initially 100 ppbv NO x, zero PAN, and zero HNO3 . The lifetime of NOx against conversion to HNO3 is 1 day. We assume that HNO 3 is removed rapidly by deposition and cannot be recycled back to NO x. We also assume [NO] << [NO 2 ] in the air parcel at all times (cf. question 1).
3.2. We now examine the effect of PAN formation, assuming a constant concentration [CH3C(O)OO] = 1x10 8 molecules cm -3 in the air parcel. Rate constants are k 4b = 4.7x10 -12 cm 3 molecule -1 s -1 and k 5 = 1.95x10 16 exp(-13,543/T).
3.2.2. Calculate the temporal evolution over a 10-day period of NO x and PAN concentrations for an air parcel transported in the boundary layer (T = 298 K). [Hint 1: assume quasi steady-state for NOx. Why is this assumption reasonable? Hint 2: you will find it convenient to define a chemical family NOx* = NOx + PAN]. What is the concentration of NO x remaining after 10 days?