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On the Climatic Relevancy of Arctic Haze: Static Energy Balance Considerations

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On the Climatic Relevancy of Arctic Haze: Static Energy Balance Considerations Tellus (1985). 37B. 50-52 SHORT CONTRIBUTION On the climatic relevancy of Arctic Haze: static energy balance considerations By GLENN E. SHAW, Geophysical Institute, University of Alaska, Fairbanks, Alaska 99701, USA (Manuscript received March 26; in final form June 29. 1984) ABSTRACT Optical properties of Arctic Haze are known only roughly, but seem to be bracketed in the following ranges: optical depth, 0.1 to 0.5; haze asymmetry factor, 0.6 to 0.7; albedo of single scattering, 0.8 to 0.98. On the basis of these numbers, simple static energy balance considera- tions suggest that the light-absorbing haze over the northern reflecting ice cap creates an earth- atmosphere warming of 0.1 to l.O°C in comparison to a hypothetical haze-free Arctic. Before elaborate climatic models can be run with such meaning, the optical properties of the Arctic Haze, its geographical extent and seasonal variation have to be determined more accurately. The intent of this note is to draw the estimated radiation absorbed by particles in the Arctic Haze, radiative and optical properties of Arctic Haze especially around the time of the vernal equinox, is together as a group and consider them in the to be expected, but in summer the haze disappears context of an extremely simple static energy because of the onset of extensive cloudiness. balance climate model. On the basis of such a “first Though the perturbation to the infrared radiation order” model it is suggested that the mean field is probably relatively small for the submicron earth-atmosphere Arctic temperature may be 0.1 to aerosols in Arctic Haze, it lasts throughout the 1 OC warmer than without haze. There is no point polar night and therefore cannot necessarily be at this time to consider more refined modeling until discounted as a potential factor in inducing climatic the radiative parameters of Arctic Haze are known alteration. We ignore the IR effects here, however. more precisely. The changes or perturbations to the “normal” After a decade of research there is now general visible-band radiative component of the polar heat agreement that the Arctic aerosol has appreciable balance (for cloudless skys) brought about by the optical thicknesses (Shaw, 1982; Mendonca et al., presence of Arctic Haze requires, ultimately, 1981) especially in spring months, and contains knowledge of at least four parameters: (I) the graphitic (i.e., black) carbon which absorbs visible- underlying surface reflectivity, A,, (2) the optical band radiation (Heintzenberg, 1982; Patterson et thickness, r, (3) the so-called haze asymmetry al., 1982: Rosen et al., 1981: Rosen and Hansen, factor, (cos(8)). and (4) the albedo of single 1984). The Arctic Haze phenomenon is, as far as scattering, ~5 of the haze-laden air. The last three we know, industrial in origin, Arctic wide in scale parameters are wavelength dependent. (Rahn and Heidam, 1981) and possibly (though The albedo of the polar surface lies in the range not certainly) has been increasing in intensity since of 0.63-0.80 in spring. Representative values for r about the time of WW I1 (Koerner and Fisher, in the Alaskan Arctic have been estimated to be 1982). -0.1 (Shaw, 1982) to 0.5 (Mendonca et al., 1981). Tropospheric warming as the result of solar The last two parameters, however, (cos (8)) and Tellus 378 (1985), 1 ON THE CLIMATIC RELEVANCY OF ARCTIC HAZE 51 wo, have unfortunately been estimated only radiation) of the Arctic around the time of vernal roughly. equinox is negative, going from about -30 W m-' On the basis of (I) measurements of down- in March to -0 by the end of April, after which welling diffuse radiation in narrow spectral band- time Arctic Haze virtually disappears. The esti- passes during episodes of Arctic Haze and (2) mated alteration in the radiative heat budget simultaneous scans of sky radiance along the solar brought about by Arctic Haze (2 to 20 W m-') is almuncatar, Shaw and Stamnes (1980) estimated therefore certainly significant in the relative sense, (cos(8)) to be between 0.6-0.8 and (3 to be but the radiative component of the heat budget is between 0.5-0.8. On the basis of (I) light absorp- fairly small. tion by soot particles collected on Nucleopore Deficits in the radiation balance in the Arctic are filters exposed at Barrow and (2) a rough know- balanced by heat from oceanic currents, latent heat ledge of aerosol size distribution and light scatter- and by the flow of sensible heat. On a yearly basis, ing, Patterson et al. (1982) estimated (cos (@) to Budyko (1974) estimates that 2.1-3.0 W m-l of be 0.67 and CI to be -0.8, but sometimes rising as heat is gained by the atmosphere from the open high as 0.9 during times of high relative humidity. leads in the polar ice and, in addition, another 2 W Finally, on the basis of (I) broad-band hemi- mr2 is gained by the latent heat at fusion of ice spheric incoming radiation measurements at Bar- taken out of the Arctic by oceanic currents (-1900 row during haze and non-haze episodes and (2) for km3 ice yrrl). As a result of oceanic circulation, several assumed aerosol size spectra, Leighton therefore, the Arctic atmosphere receives an annual (1983) deduced (by radiative transfer calculations) mean amount of-4 W m2,but the annual mean that the imaginary index of refraction for Arctic radiative deficit is much larger at about 110 W mr2. haze must be -0.01 to 0.03, with the lower value For most intents and purposes the negative being more probable. These data would suggest radiation balance of the earth-atmosphere system that w > 0.9. Clark et al. (1984) report values for in the Arctic is compensated by meridional heat single scattering albedo during spring, 1983, as transfer in the atmosphere, which we model by a 0.77 < w < 0.93 with an average of 0.86. simple conduction parameterization Putting the (admittedly very few and quite R = E(T(()- T), (1) diverse) data all together, the magnitude of the radiative parameters can be bracketed as follows: where R is the annually-averaged radiation 0.6 < A,, < 0.8; 0.1 < 5 (0.55~)< 0.5; 0.6 < cos (8) balance, T is the annual hemispheric mean tem- < 0.7; 0.8 < 6 < 0.98. The most uncertain of the perature, T(4)is the annual mean zonally-averaged four parameters, for the purposes of estimating temperature at latitude 4 and E is a constant. possible climatic change, is the parameter (3. Budyko estimates E - 3.8 W m-* K-'. At 72O North, radiative perturbation of Arctic As was pointed out, the presence of Arctic Haze Haze around the spring equinox was calculated for will increase R by 2-20 W m-2, but only during the the range of parameters stated (see Shaw and 2 months in spring (March and April), which would Stamnes, 1980) and leads to an increased mean- be equivalent to increasing the annual-average of R monthly amount of absorbed solar radiation of 2 to by 0.3 to 3%. From eq. (I), the annual mean 20 W mr2 in the lower (one or two kilometers) temperature at latitudes 72' N would rise by -0.1 troposphere; similarly there would be a radiative to 1 "C. cooling at the surface about one third the magni- A temperature change of 0.1 to 1 OC, with no tude of the tropospheric warming. This, in effect, is compensating feedback, would change the mean equivalent to reducing the effective albedo of the annual boundary of the Arctic ice northward by a earth near latitude 72ON by 2 to 8% during few to a few tens of kilometers according to the episodes of Arctic Haze around the time of vernal present meridional temperature gradient. Before equinox. Reductions in effective albedo of this one can say anything more conclusively, climatic magnitude have been documented by radiation models incorporating the dynamics and feedback measurements carried out by Valero et al. (1984). mechanisms have to be run, but right now the Now the average radiation balance (algebraic greatest need seems to be to sharpen our knowledge sum of incoming and outgoing solar and terrestrial of the parameters woand (cos (6)). Tellus 37B (1985). 1 52 G. E. SHAW REFERENCES Budyko, M. 1. 1974. Climate and Life, International 1982. Radiative properties of the Arctic aerosol. Geophysics Series, Academic Press, New York, 18, Atmos. Environ. 16, 2967-2977. 508 p. Rahn, K. A. and Heidam, N. Z. 1981. Progress i.1 Clarke, A. D., Charlson, R. J. and Radke, L. F. 1984. Arctic air chemistry, 1977-1980: a comparison of the Optical Properties of Arctic Haze, Airborne Observa- first and second symposia. Atmos. Environ. 15, tions of Arctic Aerosol, Geophys. Res. Lett. 11, 1234-1 348. 405408. Rosen, H., Navakov, T. and Bodhaine, B. A. 1981. Soot Heintzenberg, J. 1982. Size-segregated measurements of in the Arctic. Atmos. Environ. 15, 1371-1374. particulate elemental carbon and aerosol light absorp- Rosen, H. and A. D. A. Hansen, 1984. Role of com- tion at remote Arctic locations. Atmos. Environ. 16, bustion-generated carbon particles in the absorption of 2461-2469. solar radiation in the Arctic Haze, Geophys. Res. Koerner, R. M. and Fisher, D. 1982. Acid snow in the Lett. 11,461-464. Canadian high Arctic. Nature 295, 137-140. Shaw, G. E. 1982. Atmospheric turbidity in the polar Leighton, H. 1983. Influence of Arctic Haze on the regions. J. Appl. Meteorol. 21, 108CL1088.
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