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Deep in homogeneous, sourcefree waters the radiance distribution
approaches a shape
that depends only on the IOPs. Moreover, the radiance
distribution at great depth decays in magnitude exactly exponentially with a decay rate
that,
once again, depends only on the IOPs. The shape
is called the asymptotic radiance
distribution, and
is called the asymptotic decay rate or the asymptotic K function.
and
depend on the wavelength
via the wavelength dependence of the IOPs; the wavelength is
omitted here for brevity. An asymptotic radiance distribution exists only if the IOPs do not
depend on depth (homogeneous water) and if there is no inelastic scatter or bioluminescence
contributing to the radiance (sourcefree water). Preisendorfer (1976)
(in Hydrologic Optics, vol.
5, page 212) and Højerslev and Zaneveld (1977)
give rigorous mathematical proofs that
and
exist for any physically realistic phase function and singlescattering albedo.
These statements imply that the directional and depth dependencies of the radiance distribution decouple at great depths. That is to say,
This in turn implies that all irradiances decay in the asymptotic regime at the same rate as the radiance. For example,
We can compute corresponding values for , , and . Clearly, each of these irradiances has the same asymptotic K function. Using these asymptotic irradiances, we can compute asymptotic values for any apparent optical property. For example, we have
Note that any normalization factor in divides out when computing AOPs. Because the asymptotic radiance is determined solely by the IOPs, it follows that any quantity computed from is also in IOP. Therefore all apparent optical properties become inherent optical properties in the asymptotic regime. The K's, 's, R's, and their ilk, which are influenced by boundary conditions near the water surface, all approach values at depth that are independent of the boundary conditions.
An integral equation for the asymptotic radianceThe obvious question is, "How do you computed the asymptotic radiance distribution and the asymptotic decay rate, given the IOPs?" One way is to recall the RTE for homogeneous, sourcefree water
and assume that the radiance has the form seen in Eq. (1). This gives an integral equation for the shape and decay rate of the asymptotic radiance distribution:
(Note that since the scattering angle depends only on , we can set in this equation, so that the result is a function only of .) This equation is often written in terms of and a nondimensional asymptotic decay rate as
Given the IOPs c and for Eq. (2) or and for Eq. (3), we can solve either of these equations for the corresponding and or . Another form of Eq. (3), often seen in the literature, is
where is the azimuthally averaged phase function
For the idealized case of isotropic scattering, and the solution of Eq. (3) has the simple form
where is normalized to 1 at (or at the nadir direction ). This has the shape of an ellipse whose major axis is oriented vertically. The corresponding value of is the solution of the transcendental equation
Kattawar and Plass (1976) obtained an analytic solution of Eq. (3) for the Rayleigh phase function . However, for other phase functions, in particular for those characteristic of oceanic waters, the solution of Eq. (2) or (3) must be obtained numerically. Solving the integral Eq. (2) is mathematically equivalent to solving a certain eigenmatrix equation for its eigenfunctions (which give ) and eigenvectors (which give ). The eigenmatrix approach is described in Light and Water (1994) section 9.6. (HydroLight uses the eigenmatrix approach to obtain its asymptotic values. The excellent agreement between the asymptotic values computed by the eigenmatrix method and the approach with depth to those values, as obtained by independent numerical solution of the RTE, is an excellent check on the correctness of the HydroLight code.)
Dependence of asymptotic values on inherent optical propertiesAs just seen, the two asymptotic properties and are determined solely by the IOPs c, and . Figure 1 shows how the nondimensional asymptotic decay rate depends on the albedo of single scattering for three phase functions. The dotted line is for the pure water phase function ; the dashed line is for a HenyeyGreenstein phase function with an asymmetry parameter g = 0.7; and the solid line is for an "averageparticle" phase function , which is typical of phase functions for oceanic particles. The squares show experimental data taken in laboratory suspensions containing milk (Timofeeva and Gorobetz, 1967). The fat globules in milk are large ( ), efficient scatterers, which explains the similarity between the milk solution and the phase function, which is typical of particleladen natural waters.
Figure 2 shows the shape of as a function of for the averageparticle phase function . Since it is the shape that is determined by the IOPs, it is customary to normalize to one for the nadir radiance direction (looking upward in the zenith direction). The viewing angle as plotted is the angle in which an underwater observer would look in order to see photons traveling in direction ; and are both measured from the , or nadir, direction. Thus, corresponds to looking toward the zenith and seeing photons heading straight down ( ). As we would expect, in highly scattering water (large ) the upwelling radiance is relatively much greater than in weakly scattering water (small ). Corresponding curves for the Rayleigh phase function can be seen in Kattawar and Plass (1976). Prieur and Morel (1971) show such curves as a function of the relative contributions by molecular and particle scattering, i.e., for phase functions that are in between and .
Figure 3 shows the asymptotic mean cosines and irradiance reflectance for the same phase functions used in Fig. 1.
Rate of approach to asymptotic valuesThe asymptotic values are determined solely by the IOPs of a homogeneous water body. However, how quickly a given quantity approaches its asymptotic value depends both on the IOPs and on the boundary conditions. We have already seen this in the discussion of K functions, but a few more examples will be instructive. HydroLight was run for Case 1 water with a chlorophyll concentration of . The wavelength was 443 nm. The corresponding IOPs (including water) were , , so that . Thus one meter of geometric depth is about 0.5 optical depths. The albedo of single scattering is then , and the total backscatter fraction was 0.1253. Figure 4 shows at 443 nm for four different surface boundary conditions:
The curves of Fig. 4 show the boundary effects on the rate of approach to the asymptotic value of , which depends only on the IOPs. The curve for the heavily overcast sky approaches the quickest. The physical reason is that the overcast sky radiance is already a diffuse radiance distribution, so that less scattering (i.e., less propagation to depth) is required to redirect the initial photon directions towards the asymptotic angular distribution within the water. The other cases with the sun in a clear sky have a strongly collimated incident radiance distribution, which requires more scattering (a deeper depth) to "erase the memory" of where the sun is in the sky and achieve the asymptotic shape of . For the 50 deg sun angle, the surface roughness makes a noticeable but minor difference.
Figure 5 shows the corresponding results for the approach of the irradiance reflectance to its asymptotic value of .
Fig. 6 shows the mean cosines , , and .
Finally, Fig. 7 shows the approach of measured and modeled radiances to the asymptotic shape. The dots are radiances measured in the azimuthal plane of the sun by Tyler (1960) at the depths indicated. The blue curves are the corresponding HydroLight simulation. The measured data were published only as relative values. Therefore, the radiances are normalized for plotting to a value of 1 in the nadirviewing direction ( ) at depth 4.2 m. The direction is looking toward the sun, and is looking away from the sun. The red curve shows the shape of , normalized to the nadirviewing measured value at 66.1 m. The data are described in detail in Tyler's report, and the modeling is described in Light and Water (1994) section 11.1. Given the uncertainties in the measured data and the educated guesses that had to be made about unmeasured inputs needed by HydroLight, the overall agreement between data and model predictions is quite good. Near the surface, the sun's location is obvious and the unscattered direct beam gives a large spike in the radiance. At 29.0 m, the sun's azimuthal direction can still be discerned, but the large spike of the direct beam has been removed by scattering. By 66.1 m, there is only a slight asymmetry remaining to indicate the sun's azimuthal direction. Clearly, both the measured and modeled radiances are close to the asymptotic shape at 66.1 m, which was about 26 optical depths.

