Diffuse sky radiation

A spectrum taken of blue sky clearly showing solar Fraunhofer lines and atmospheric water absorption band.

Diffuse sky radiation is solar radiation reaching the Earth's surface after having been scattered from the direct solar beam by molecules or suspensoids in the atmosphere. It is also called skylight, diffuse skylight, or sky radiation and is the reason for changes in the color of the sky. Of the total light removed from the direct solar beam by scattering in the atmosphere (approximately 25% of the incident radiation when the sun is high in the sky, depending on the amount of dust and haze in the atmosphere), about two-thirds ultimately reaches the earth as diffuse sky radiation. When the sun is at the zenith in a cloudless sky, with 1367 W/m² above the atmosphere, direct sunlight is about 1050 W/m², and total insolation about 1120 W/m².^[1] This implies that under these conditions the diffuse radiation is only about 70 W/m² out of the original 1367 W/m².

The important processes in the atmosphere (Rayleigh scattering and Mie scattering) are elastic processes, by which light can be deviated from its path without being absorbed and with no change in wavelength.

Colour

Clear blue sky.

Comparison of the scattering efficiency of blue light in the atmosphere compared to red light.

The sunlit sky is blue because air scatters short-wavelength light more than longer wavelengths. Since blue light is at the short wavelength end of the visible spectrum, it is more strongly scattered in the atmosphere than long wavelength red light. The result is that the human eye perceives blue when looking toward parts of the sky other than the sun.^[2] The color perceived is similar to that obtained by a monochromatic blue of wavelength 474–476 nm mixed with white light, i.e., an unsaturated blue light.^[3]

Near sunrise and sunset, most of the light we see comes in nearly tangentially to the Earth's surface; thus, the light's path through the atmosphere is so long that much of the blue and even green light is scattered out, leaving the sun rays and the clouds it illuminates red. Therefore, when looking at the sunset and sunrise, we see the colour red more than the other colors.

Scattering and absorption are major causes of the attenuation of radiation by the atmosphere. Scattering varies as a function of the ratio of the particle diameter to the wavelength of the radiation. When this ratio is less than about one-tenth, Rayleigh scattering occurs in which the scattering coefficient varies inversely as the fourth power of the wavelength. At larger values of the ratio of particle diameter to wavelength, the scattering varies in a complex fashion described, for spherical particles, by the Mie theory; at a ratio of the order of 10, the laws of geometric optics begin to apply.

In the example of the sky at the zenith, it is blue during broad daylight due to Rayleigh scattering involving diatomic gases (N
2, O
2). Near sunset and especially during twilight, ozone (O
3) absorption significantly contributes to maintaining the blue sky color.

Neutral points

There are four commonly detectable points of zero polarization of diffuse sky radiation (known as neutral points) lying along the vertical circle through the sun.

• The Arago point, named after its discoverer, is customarily located at about 20° above the antisolar point; but it lies at higher altitudes in turbid air. The latter property makes the Arago distance a useful measure of atmospheric turbidity.
• The Babinet point, discovered by Babinet in 1840, is located about 15° to 20° above the sun, hence it is difficult to observe because of solar glare.
• The Brewster point, discovered by Brewster in 1840, is located about 15° to 20° below the sun; hence it is difficult to observe because of solar glare.
• The fourth point, located at about 20° below the antisolar point, visible only at higher altitudes in the air or space^[4]

Under an overcast sky

There is essentially no direct sunlight under an overcast sky, so all light is then diffuse sky radiation. The flux of light is not very wavelength dependent because the cloud droplets are larger than the light's wavelength and scatter all colors approximately equally. The light passes through the translucent clouds in a manner similar to frosted glass. The intensity ranges (roughly) from ¹⁄₆ of direct sunlight for relatively thin clouds down to ¹⁄₁₀₀₀ of direct sunlight under the extreme of thickest storm clouds.

See also

• Atmospheric diffraction
• Aerial perspective
• Cyanometer
• Daylight
• Nighttime airglow
• Tyndall effect
• Rayleigh scattering
• Rayleigh Sky Model

References

1. "Introduction to Solar Radiation". Newport Corporation. Archived from the original on Oct 29, 2013.
2. "Rayleigh scattering." Encyclopædia Britannica. 2007. Encyclopædia Britannica Online. 16 Nov. 2007.
3. "Human color vision and the unsaturated blue colour of the daytime sky", Glenn S. Smith, American Journal of Physics, Volume 73, Issue 7, pp. 590-597 (2005).
4. Horváth G, Bernáth B, Suhai B, Barta A, Wehner R.: First observation of the fourth neutral polarization point in the atmosphere, J Opt Soc Am A Opt Image Sci Vis. 2002 Oct;19(10):2085-99.

Further reading

• Pesic, Peter (2005). Sky in a Bottle. The MIT Press. ISBN 978-0-262-16234-0.

External links

• Dr. C. V. Raman lecture: Why is the sky blue?
• Why is the sky blue?
• Blue Sky and Rayleigh Scattering
• Atmospheric Optics (.pdf), Dr. Craig Bohren