Page updated: April 12, 2020
Author: Curtis Mobley
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Energy Conservation

When making radiance or irradiance measurements in the ocean, it is sometimes hard to verify that energy is being conserved. This is equally true when looking at the output from a numerical model such as HydroLight. Confusion most often arises when comparing measurements made just above and below the sea surface and observing that the measured (or predicted) radiances do not seem to ”add up” correctly. To resolve such confusion, first note that it’s the Law of Conservation of Energy, not the law of conservation of radiance or irradiance. We must therefore express the law of conservation of energy in terms of radiance or irradiance as appropriate to the measurements being made.

Within the Water

Within the water column, if there are no internal sources such as bioluminescence or inelastic scatter contributing to the wavelength of interest, conservation of energy is expressed in terms of irradiances by Gershun’s law:

a(z,λ) = 1 Eo(z,λ) d[Ed(z,λ) Eu(z,λ)] dz . (1)

Here a is the absorption coefficient, Eo is the scalar irradiance, and Ed and Eu are the downwelling and upwelling plane irradiances. This equation can be illustrated using numerical results generated by HydroLight. A run was made with the sun placed at a 60 deg zenith angle in a clear sky; the wind speed was 5ms1, and the water was infinitely deep. The absorption coefficient was set to a = 0.1m1, the scattering coefficient to b = 0.4m1, and an ”average-particle” phase function was chosen. (The run used HydroLight’s ”abconst” IOP model for these inputs.) No internal sources were included in the run. Table 1 shows the computed irradiances at depths of 5.00 and 5.01 m. Closely spaced depths are used to illustrate Eq. (1) so that the depth derivative can be accurately approximated as a finite difference and the scalar irradiance can be taken as the average of the values at 5.00 and 5.01 m.






depth (m)EoEuEd




5.00 0.51833 0.013151 0.32613




5.01 0.51749 0.013129 0.32559





Table 1: Tab. 1. Irradiances computed within the water body as described in the text. Irradiances have units of Wm2nm1.

Using these values in the finite difference approximation of Eq. (1) gives

a = 1 0.5(0.51833 + 0.51749)(0.32559 0.013129) (0.32613 0.013151) 5.01 5.00 = 0.1000m1.

The absorption coefficient as computed from the irradiances via Gershun’s law is the same as the one used as input to the run, so HydroLight is conserving energy in its in-water solution of the radiative transfer equation. (HydroLight also conserves energy if internal sources are present. Demonstration of that requires adding an appropriate source term to Gershun’s equation; see Light and Water (1994) Eq. 5.34.) Such accuracy cannot be expected with real data because of imperfect instrument calibration and other sources of error such as Raman scatter (an internal source not accounted for in Eq. 1), which will always be present to some degree during daylight measurements. Nevertheless, Gershun’s law can be a useful way to retrieve absorption coefficients from in-water radiance or irradiance measurements, as seen in papers by Voss (1989) and Maffione et al. (1993).

Across the Air-Water Surface

The situation is more complicated when considering energy conservation across the air-water surface. Consider a collimated beam of light incident onto a level sea surface. Part will be reflected and part will be transmitted into the water. Figure 1 shows this geometry and various quantities needed to express conservation of energy at the surface.


PIC

Figure 1: Fig. 1. Geometry needed for expressing the law of conservation of energy in terms of irradiances across a level sea surface.

Conservation of energy (or equivalently, power) across the surface requires that

Pi = Pr + Pt, (2)

where Pi is the power in an incident collimated beam of cross section Ai, Pr is the power in the reflected beam of cross section Ar, and Pt is the power in transmitted beam of cross section At. These beam cross sectional areas are shown in green in Fig. 1. The beam of incident power illuminates a horizontal area As of the level sea surface (shown in blue).

Conservation in terms of plane irradiances

Conservation of energy can be expressed in terms of incident (downwelling), reflected (upwelling), and transmitted (downwelling) plane irradiances using the horizontal projections of the beam cross section areas. Recalling that plane irradiance is power per unit horizontal area, Eq. (2) becomes

ApEd(incident,inair) = ApEu(reflected,inair) + ApEd(transmitted,inwater),

where the horizontally projected areas Ap corresponding to each beam are shown in yellow in Fig. 1. Since each beam has the same horizontally projected area, this equation reduces to just

Ed(incident,inair) = Eu(reflected,inair) + Ed(transmitted,inwater). (3)

Equation (3) is conservation of energy across the surface expressed in terms of plane irradiances for a collimated incident beam.

Conservation in terms of scalar irradiances

To express Eq. (2) in terms of the scalar irradiances, first recall how Eod is obtained from the radiance (Eq 5 of the Geometrical Radiometry page):

Eod = 2πdL(ξ̂)dΩ(ξ̂).

For a collimated incident beam in direction ξo ̂, we can write the radiance in terms of the beam irradiance and a Dirac delta function to get

Eod = 2πdEδ(ξ̂ ξ o ̂)dΩ(ξ̂) = E ,

where E is the incident irradiance on the beam cross sectional area; E = PiAi. Similar equations hold for the reflected and transmitted scalar irradiances. These beam cross sectional areas are shown in green in Fig. 1. Thus Eq. (2) becomes

AiEod(incident,inair) = ArEou(reflected,inair) + AtEod(transmitted,inwater),

or

Eod(incident,inair) = Eou(reflected,inair) + AtEod(transmitted,inwater)At Ai, (4)

after noting that Ar = Ai by the law of reflection. By geometry, the ratio of areas AtAi is just cos𝜃tcos𝜃i. 𝜃t can be written in terms of 𝜃i using Snell’s law, sin𝜃i = nsin𝜃t, where n is the real index of refraction of the water. Equation (4) then becomes

Eod(incident,inair) = Eou(reflected,inair) + Eod(transmitted,inwater) 1 cos𝜃i1 sin 2 𝜃i n2 . (5) 

Equation (5) is conservation of energy expressed in terms of scalar irradiance for a collimated incident beam.

To illustrate Equations (3) and (5) with HydroLight output, a run was made with the sun at a zenith angle of 𝜃i = 60deg in a black sky, in order to obtain a collimated incident beam. The incident Ed onto the surface was set to 1. The sea surface was level (zero wind speed), and the water index of refraction was n = 1.34. The scattering coefficient within in the water was set to zero, so that upwelling light from the water column would not confuse the illustration of energy conservation across the sea surface itself. The absorption coefficient was set to a = 0.1m1. (These runs used HydroLight IOP model ”abconst” and the ”idealized sky model”).

The computed irradiances just above and below the surface are shown in Table 2. The upwelling irradiances in the water are zero because there was no scattering by the water and the bottom was infinitely deep. These computed irradiances satisfy Equations (3) and (5), showing that HydroLight conserves energy across the surface.







location EouEodEuEd





in air 0.12690 2.0077 0.063209 1.0000





in water at depth 00.00000 1.2277 0.0000 0.93693






Table 2: Tab. 2. Plane and scalar irradiances for a collimated incident beam and no scattering within the water.

A run was then done with a heavily overcast sky to generate a diffuse sky radiance pattern with the sun’s location not discernable. The wind speed was 10ms1 to generate a non-level sea surface. The resulting irradiances are shown in Table 3.







location EouEodEuEd





in air 0.18863 1.7764 0.050456 1.0000





in water at depth 00.00000 1.1430 0.0000 0.94954






Table 3: Tab. 3. Plane and scalar irradiances for a diffuse incident sky radiance and no scattering within the water.

As before, these plane irradiances satisfy Eq. (3). However, the scalar irradiances do not satisfy Eq. (5). The reason is that Eq. (5) must be applied for each particular incident direction 𝜃i of the diffuse sky radiance, in order to correctly compute the angle factor seen in Eq. (5). If this is done one direction at a time (with the sun in a black sky), each individual incident direction satisfies Eq. (5) just as in the previous example. Thus energy in conserved across the surface ”beam by beam,” hence in toto, even if it is not obvious from the total scalar irradiances.

A further complication occurs when the water body has scattering. To illustrate this, the scattering coefficient was set to b = 0.4m1 and an ”average-particle” phase function was used in the previous simulation. The computed irradiance were then







location EouEodEuEd





in air 0.21264 1.7764 0.062372 1.0000





in water at depth 00.07922 1.2046 0.031115 0.96873






Table 4: Tab 4: Plane and scalar irradiances for a diffuse incident radiance, with scattering in the water.

Now even the plane irradiance appears to violate conservation of energy, Eq. (3). The reason is that Eou and Eu in air contain both surface-reflected radiance (as before) and radiance transmitted upward through the sea surface. Likewise, Eod and Ed in the water contain both downward transmitted irradiance (as before) as well as upwelling radiance that has been reflected back downward by the surface. This makes it appear at first glance that the irradiances do not add up correctly, even though energy actually is conserved across the air-water surface. The effects of both the surface itself and the water body can be accounted for simply by tallying the plane irradiances incident onto and leaving the surface from above and below:

Ed(downwelling,inair) Eu(upwelling,inair) = Ed(downwelling,inwater) Eu(upwelling,inwater). (6)

Equation (6) expresses conservation of energy for the surface plus water body, for any conditions of incident lighting and water IOPs. The irradiances seen in Table 4 satisfy this equation.

Conservation in terms of radiance

Another complication occurs when expressing conservation of energy across the surface in terms of radiance. Now it is necessary to account for changes in both the beam cross sectional area and in solid angle when going across the surface. When interpreting HydroLight output, it must be remembered that the computed radiances are averages over ”quads” or solid angles of finite size, as discussed on the HydroLight page. Such quads are represented by the green areas in Fig. 2.


PIC

Figure 2: Fig. 2. Illustration of the HydroLight radiance quads as needed to express energy conservation for a collimated beam across a level sea surface.

Remembering that radiance is power per unit area per unit solid angle, Eq. (2) can be written as

LiAiΔΩi = LrArΔΩr + LtAtΔΩt,

or

Li = Lr + Lt AtΔΩt Ai,ΔΩi,

after noting that Ar = Ai and ΔΩr = ΔΩi by the law of reflection. As noted before, AtAi = cos𝜃tcos𝜃i. The solid angles are given by ΔΩ = Δ(cos𝜃)Δϕ, where the angle ranges are determined by the 𝜃 and ϕ boundaries of the quads. Thus the last equation becomes

Li = Lr + Lt cos𝜃t cos𝜃iΔ(cos𝜃t) Δ(cos𝜃i), (7)

since Δϕt = Δϕi for the HydroLight quad layout. These angle factors must be evaluated for the particular quads associated with the incident and transmitted beams.

Consider again the previous case of the sun in a black sky at 𝜃i = 60deg, a level water surface, and no scattering. The incident and reflected HydroLight quads are centered at 60 deg and extend from 55 to 65 deg. Snell’s law gives the transmitted direction as 𝜃t = sin1[(sin𝜃i)n] = 40.26deg. Thus the transmitted radiance is contained in the HydroLight quad centered at 40 deg and extending from 35 to 45 deg. For the transmitted quad, for example, Δ(cos𝜃t) = cos35 cos45 = 0.11205. Evaluating the angle factors in Eq. (7) for these quads gives

Li = Lr + Lt0.76604 0.500000.11205 0.15096. (8)

The corresponding computed quad-averaged radiances for this run were Li = 50.7996, Lr = 3.21094, and Lt = 41.8544Wm2sr1nm1. These radiances satisfy Eq. (8). Thus energy expressed as radiance is conserved beam-by-beam across the water surface.

We have seen that conservation of energy across the sea surface can be expressed in various ways in terms of radiance and irradiance. However, those expressions are often written for collimated incident beams and consider only the surface itself (Eqs. 3, 5, and 7). It is therefore not always obvious that energy is conserved for the entire surface plus water column when looking at data or simulations for realistic conditions of sky radiances and water IOPs. In general, Eq. (6) should be used to check conservation of energy across the sea surface with measured or modeled plane irradiances.

When making radiance or irradiance measurements in the ocean, it is sometimes hard to verify that energy is being conserved. This is equally true when looking at the output from a numerical model such as HydroLight. Confusion most often arises when comparing measurements made just above and below the sea surface and observing that the measured (or predicted) radiances do not seem to ”add up” correctly. To resolve such confusion, first note that it’s the Law of Conservation of Energy, not the law of conservation of radiance or irradiance. We must therefore express the law of conservation of energy in terms of radiance or irradiance as appropriate to the measurements being made.

Within the Water

Within the water column, if there are no internal sources such as bioluminescence or inelastic scatter contributing to the wavelength of interest, conservation of energy is expressed in terms of irradiances by Gershun’s law:

a(z,λ) = 1 Eo(z,λ) d[Ed(z,λ) Eu(z,λ)] dz . (1)

Here a is the absorption coefficient, Eo is the scalar irradiance, and Ed and Eu are the downwelling and upwelling plane irradiances. This equation can be illustrated using numerical results generated by HydroLight. A run was made with the sun placed at a 60 deg zenith angle in a clear sky; the wind speed was 5ms1, and the water was infinitely deep. The absorption coefficient was set to a = 0.1m1, the scattering coefficient to b = 0.4m1, and an ”average-particle” phase function was chosen. (The run used HydroLight’s ”abconst” IOP model for these inputs.) No internal sources were included in the run. Table 1 shows the computed irradiances at depths of 5.00 and 5.01 m. Closely spaced depths are used to illustrate Eq. (1) so that the depth derivative can be accurately approximated as a finite difference and the scalar irradiance can be taken as the average of the values at 5.00 and 5.01 m.






depth (m)EoEuEd




5.00 0.51833 0.013151 0.32613




5.01 0.51749 0.013129 0.32559





Table 1: Tab. 1. Irradiances computed within the water body as described in the text. Irradiances have units of Wm2nm1.

Using these values in the finite difference approximation of Eq. (1) gives

a = 1 0.5(0.51833 + 0.51749)(0.32559 0.013129) (0.32613 0.013151) 5.01 5.00 = 0.1000m1.

The absorption coefficient as computed from the irradiances via Gershun’s law is the same as the one used as input to the run, so HydroLight is conserving energy in its in-water solution of the radiative transfer equation. (HydroLight also conserves energy if internal sources are present. Demonstration of that requires adding an appropriate source term to Gershun’s equation; see Light and Water (1994) Eq. 5.34.) Such accuracy cannot be expected with real data because of imperfect instrument calibration and other sources of error such as Raman scatter (an internal source not accounted for in Eq. 1), which will always be present to some degree during daylight measurements. Nevertheless, Gershun’s law can be a useful way to retrieve absorption coefficients from in-water radiance or irradiance measurements, as seen in papers by Voss (1989) and Maffione et al. (1993).

Across the Air-Water Surface

The situation is more complicated when considering energy conservation across the air-water surface. Consider a collimated beam of light incident onto a level sea surface. Part will be reflected and part will be transmitted into the water. Figure 1 shows this geometry and various quantities needed to express conservation of energy at the surface.


PIC

Figure 1: Fig. 1. Geometry needed for expressing the law of conservation of energy in terms of irradiances across a level sea surface.

Conservation of energy (or equivalently, power) across the surface requires that

Pi = Pr + Pt, (2)

where Pi is the power in an incident collimated beam of cross section Ai, Pr is the power in the reflected beam of cross section Ar, and Pt is the power in transmitted beam of cross section At. These beam cross sectional areas are shown in green in Fig. 1. The beam of incident power illuminates a horizontal area As of the level sea surface (shown in blue).

Conservation in terms of plane irradiances

Conservation of energy can be expressed in terms of incident (downwelling), reflected (upwelling), and transmitted (downwelling) plane irradiances using the horizontal projections of the beam cross section areas. Recalling that plane irradiance is power per unit horizontal area, Eq. (2) becomes

ApEd(incident,inair) = ApEu(reflected,inair) + ApEd(transmitted,inwater),

where the horizontally projected areas Ap corresponding to each beam are shown in yellow in Fig. 1. Since each beam has the same horizontally projected area, this equation reduces to just

Ed(incident,inair) = Eu(reflected,inair) + Ed(transmitted,inwater). (3)

Equation (3) is conservation of energy across the surface expressed in terms of plane irradiances for a collimated incident beam.

Conservation in terms of scalar irradiances

To express Eq. (2) in terms of the scalar irradiances, first recall how Eod is obtained from the radiance (Eq 5 of the Geometrical Radiometry page):

Eod = 2πdL(ξ̂)dΩ(ξ̂).

For a collimated incident beam in direction ξo ̂, we can write the radiance in terms of the beam irradiance and a Dirac delta function to get

Eod = 2πdEδ(ξ̂ ξ o ̂)dΩ(ξ̂) = E ,

where E is the incident irradiance on the beam cross sectional area; E = PiAi. Similar equations hold for the reflected and transmitted scalar irradiances. These beam cross sectional areas are shown in green in Fig. 1. Thus Eq. (2) becomes

AiEod(incident,inair) = ArEou(reflected,inair) + AtEod(transmitted,inwater),

or

Eod(incident,inair) = Eou(reflected,inair) + AtEod(transmitted,inwater)At Ai, (4)

after noting that Ar = Ai by the law of reflection. By geometry, the ratio of areas AtAi is just cos𝜃tcos𝜃i. 𝜃t can be written in terms of 𝜃i using Snell’s law, sin𝜃i = nsin𝜃t, where n is the real index of refraction of the water. Equation (4) then becomes

Eod(incident,inair) = Eou(reflected,inair) + Eod(transmitted,inwater) 1 cos𝜃i1 sin 2 𝜃i n2 . (5) 

Equation (5) is conservation of energy expressed in terms of scalar irradiance for a collimated incident beam.

To illustrate Equations (3) and (5) with HydroLight output, a run was made with the sun at a zenith angle of 𝜃i = 60deg in a black sky, in order to obtain a collimated incident beam. The incident Ed onto the surface was set to 1. The sea surface was level (zero wind speed), and the water index of refraction was n = 1.34. The scattering coefficient within in the water was set to zero, so that upwelling light from the water column would not confuse the illustration of energy conservation across the sea surface itself. The absorption coefficient was set to a = 0.1m1. (These runs used HydroLight IOP model ”abconst” and the ”idealized sky model”).

The computed irradiances just above and below the surface are shown in Table 2. The upwelling irradiances in the water are zero because there was no scattering by the water and the bottom was infinitely deep. These computed irradiances satisfy Equations (3) and (5), showing that HydroLight conserves energy across the surface.







location EouEodEuEd





in air 0.12690 2.0077 0.063209 1.0000





in water at depth 00.00000 1.2277 0.0000 0.93693






Table 2: Tab. 2. Plane and scalar irradiances for a collimated incident beam and no scattering within the water.

A run was then done with a heavily overcast sky to generate a diffuse sky radiance pattern with the sun’s location not discernable. The wind speed was 10ms1 to generate a non-level sea surface. The resulting irradiances are shown in Table 3.







location EouEodEuEd





in air 0.18863 1.7764 0.050456 1.0000





in water at depth 00.00000 1.1430 0.0000 0.94954






Table 3: Tab. 3. Plane and scalar irradiances for a diffuse incident sky radiance and no scattering within the water.

As before, these plane irradiances satisfy Eq. (3). However, the scalar irradiances do not satisfy Eq. (5). The reason is that Eq. (5) must be applied for each particular incident direction 𝜃i of the diffuse sky radiance, in order to correctly compute the angle factor seen in Eq. (5). If this is done one direction at a time (with the sun in a black sky), each individual incident direction satisfies Eq. (5) just as in the previous example. Thus energy in conserved across the surface ”beam by beam,” hence in toto, even if it is not obvious from the total scalar irradiances.

A further complication occurs when the water body has scattering. To illustrate this, the scattering coefficient was set to b = 0.4m1 and an ”average-particle” phase function was used in the previous simulation. The computed irradiance were then







location EouEodEuEd





in air 0.21264 1.7764 0.062372 1.0000





in water at depth 00.07922 1.2046 0.031115 0.96873






Table 4: Tab 4: Plane and scalar irradiances for a diffuse incident radiance, with scattering in the water.

Now even the plane irradiance appears to violate conservation of energy, Eq. (3). The reason is that Eou and Eu in air contain both surface-reflected radiance (as before) and radiance transmitted upward through the sea surface. Likewise, Eod and Ed in the water contain both downward transmitted irradiance (as before) as well as upwelling radiance that has been reflected back downward by the surface. This makes it appear at first glance that the irradiances do not add up correctly, even though energy actually is conserved across the air-water surface. The effects of both the surface itself and the water body can be accounted for simply by tallying the plane irradiances incident onto and leaving the surface from above and below:

Ed(downwelling,inair) Eu(upwelling,inair) = Ed(downwelling,inwater) Eu(upwelling,inwater). (6)

Equation (6) expresses conservation of energy for the surface plus water body, for any conditions of incident lighting and water IOPs. The irradiances seen in Table 4 satisfy this equation.

Conservation in terms of radiance

Another complication occurs when expressing conservation of energy across the surface in terms of radiance. Now it is necessary to account for changes in both the beam cross sectional area and in solid angle when going across the surface. When interpreting HydroLight output, it must be remembered that the computed radiances are averages over ”quads” or solid angles of finite size, as discussed on the HydroLight page. Such quads are represented by the green areas in Fig. 2.


PIC

Figure 2: Fig. 2. Illustration of the HydroLight radiance quads as needed to express energy conservation for a collimated beam across a level sea surface.

Remembering that radiance is power per unit area per unit solid angle, Eq. (2) can be written as

LiAiΔΩi = LrArΔΩr + LtAtΔΩt,

or

Li = Lr + Lt AtΔΩt Ai,ΔΩi,

after noting that Ar = Ai and ΔΩr = ΔΩi by the law of reflection. As noted before, AtAi = cos𝜃tcos𝜃i. The solid angles are given by ΔΩ = Δ(cos𝜃)Δϕ, where the angle ranges are determined by the 𝜃 and ϕ boundaries of the quads. Thus the last equation becomes

Li = Lr + Lt cos𝜃t cos𝜃iΔ(cos𝜃t) Δ(cos𝜃i), (7)

since Δϕt = Δϕi for the HydroLight quad layout. These angle factors must be evaluated for the particular quads associated with the incident and transmitted beams.

Consider again the previous case of the sun in a black sky at 𝜃i = 60deg, a level water surface, and no scattering. The incident and reflected HydroLight quads are centered at 60 deg and extend from 55 to 65 deg. Snell’s law gives the transmitted direction as 𝜃t = sin1[(sin𝜃i)n] = 40.26deg. Thus the transmitted radiance is contained in the HydroLight quad centered at 40 deg and extending from 35 to 45 deg. For the transmitted quad, for example, Δ(cos𝜃t) = cos35 cos45 = 0.11205. Evaluating the angle factors in Eq. (7) for these quads gives

Li = Lr + Lt0.76604 0.500000.11205 0.15096. (8)

The corresponding computed quad-averaged radiances for this run were Li = 50.7996, Lr = 3.21094, and Lt = 41.8544Wm2sr1nm1. These radiances satisfy Eq. (8). Thus energy expressed as radiance is conserved beam-by-beam across the water surface.

We have seen that conservation of energy across the sea surface can be expressed in various ways in terms of radiance and irradiance. However, those expressions are often written for collimated incident beams and consider only the surface itself (Eqs. 3, 5, and 7). It is therefore not always obvious that energy is conserved for the entire surface plus water column when looking at data or simulations for realistic conditions of sky radiances and water IOPs. In general, Eq. (6) should be used to check conservation of energy across the sea surface with measured or modeled plane irradiances.

When making radiance or irradiance measurements in the ocean, it is sometimes hard to verify that energy is being conserved. This is equally true when looking at the output from a numerical model such as HydroLight. Confusion most often arises when comparing measurements made just above and below the sea surface and observing that the measured (or predicted) radiances do not seem to ”add up” correctly. To resolve such confusion, first note that it’s the Law of Conservation of Energy, not the law of conservation of radiance or irradiance. We must therefore express the law of conservation of energy in terms of radiance or irradiance as appropriate to the measurements being made.

Within the Water

Within the water column, if there are no internal sources such as bioluminescence or inelastic scatter contributing to the wavelength of interest, conservation of energy is expressed in terms of irradiances by Gershun’s law:

a(z,λ) = 1 Eo(z,λ) d[Ed(z,λ) Eu(z,λ)] dz . (1)

Here a is the absorption coefficient, Eo is the scalar irradiance, and Ed and Eu are the downwelling and upwelling plane irradiances. This equation can be illustrated using numerical results generated by HydroLight. A run was made with the sun placed at a 60 deg zenith angle in a clear sky; the wind speed was 5ms1, and the water was infinitely deep. The absorption coefficient was set to a = 0.1m1, the scattering coefficient to b = 0.4m1, and an ”average-particle” phase function was chosen. (The run used HydroLight’s ”abconst” IOP model for these inputs.) No internal sources were included in the run. Table 1 shows the computed irradiances at depths of 5.00 and 5.01 m. Closely spaced depths are used to illustrate Eq. (1) so that the depth derivative can be accurately approximated as a finite difference and the scalar irradiance can be taken as the average of the values at 5.00 and 5.01 m.






depth (m)EoEuEd




5.00 0.51833 0.013151 0.32613




5.01 0.51749 0.013129 0.32559





Table 1: Tab. 1. Irradiances computed within the water body as described in the text. Irradiances have units of Wm2nm1.

Using these values in the finite difference approximation of Eq. (1) gives

a = 1 0.5(0.51833 + 0.51749)(0.32559 0.013129) (0.32613 0.013151) 5.01 5.00 = 0.1000m1.

The absorption coefficient as computed from the irradiances via Gershun’s law is the same as the one used as input to the run, so HydroLight is conserving energy in its in-water solution of the radiative transfer equation. (HydroLight also conserves energy if internal sources are present. Demonstration of that requires adding an appropriate source term to Gershun’s equation; see Light and Water (1994) Eq. 5.34.) Such accuracy cannot be expected with real data because of imperfect instrument calibration and other sources of error such as Raman scatter (an internal source not accounted for in Eq. 1), which will always be present to some degree during daylight measurements. Nevertheless, Gershun’s law can be a useful way to retrieve absorption coefficients from in-water radiance or irradiance measurements, as seen in papers by Voss (1989) and Maffione et al. (1993).

Across the Air-Water Surface

The situation is more complicated when considering energy conservation across the air-water surface. Consider a collimated beam of light incident onto a level sea surface. Part will be reflected and part will be transmitted into the water. Figure 1 shows this geometry and various quantities needed to express conservation of energy at the surface.


PIC

Figure 1: Fig. 1. Geometry needed for expressing the law of conservation of energy in terms of irradiances across a level sea surface.

Conservation of energy (or equivalently, power) across the surface requires that

Pi = Pr + Pt, (2)

where Pi is the power in an incident collimated beam of cross section Ai, Pr is the power in the reflected beam of cross section Ar, and Pt is the power in transmitted beam of cross section At. These beam cross sectional areas are shown in green in Fig. 1. The beam of incident power illuminates a horizontal area As of the level sea surface (shown in blue).

Conservation in terms of plane irradiances

Conservation of energy can be expressed in terms of incident (downwelling), reflected (upwelling), and transmitted (downwelling) plane irradiances using the horizontal projections of the beam cross section areas. Recalling that plane irradiance is power per unit horizontal area, Eq. (2) becomes

ApEd(incident,inair) = ApEu(reflected,inair) + ApEd(transmitted,inwater),

where the horizontally projected areas Ap corresponding to each beam are shown in yellow in Fig. 1. Since each beam has the same horizontally projected area, this equation reduces to just

Ed(incident,inair) = Eu(reflected,inair) + Ed(transmitted,inwater). (3)

Equation (3) is conservation of energy across the surface expressed in terms of plane irradiances for a collimated incident beam.

Conservation in terms of scalar irradiances

To express Eq. (2) in terms of the scalar irradiances, first recall how Eod is obtained from the radiance (Eq 5 of the Geometrical Radiometry page):

Eod = 2πdL(ξ̂)dΩ(ξ̂).

For a collimated incident beam in direction ξo ̂, we can write the radiance in terms of the beam irradiance and a Dirac delta function to get

Eod = 2πdEδ(ξ̂ ξ o ̂)dΩ(ξ̂) = E ,

where E is the incident irradiance on the beam cross sectional area; E = PiAi. Similar equations hold for the reflected and transmitted scalar irradiances. These beam cross sectional areas are shown in green in Fig. 1. Thus Eq. (2) becomes

AiEod(incident,inair) = ArEou(reflected,inair) + AtEod(transmitted,inwater),

or

Eod(incident,inair) = Eou(reflected,inair) + AtEod(transmitted,inwater)At Ai, (4)

after noting that Ar = Ai by the law of reflection. By geometry, the ratio of areas AtAi is just cos𝜃tcos𝜃i. 𝜃t can be written in terms of 𝜃i using Snell’s law, sin𝜃i = nsin𝜃t, where n is the real index of refraction of the water. Equation (4) then becomes

Eod(incident,inair) = Eou(reflected,inair) + Eod(transmitted,inwater) 1 cos𝜃i1 sin 2 𝜃i n2 . (5) 

Equation (5) is conservation of energy expressed in terms of scalar irradiance for a collimated incident beam.

To illustrate Equations (3) and (5) with HydroLight output, a run was made with the sun at a zenith angle of 𝜃i = 60deg in a black sky, in order to obtain a collimated incident beam. The incident Ed onto the surface was set to 1. The sea surface was level (zero wind speed), and the water index of refraction was n = 1.34. The scattering coefficient within in the water was set to zero, so that upwelling light from the water column would not confuse the illustration of energy conservation across the sea surface itself. The absorption coefficient was set to a = 0.1m1. (These runs used HydroLight IOP model ”abconst” and the ”idealized sky model”).

The computed irradiances just above and below the surface are shown in Table 2. The upwelling irradiances in the water are zero because there was no scattering by the water and the bottom was infinitely deep. These computed irradiances satisfy Equations (3) and (5), showing that HydroLight conserves energy across the surface.







location EouEodEuEd





in air 0.12690 2.0077 0.063209 1.0000





in water at depth 00.00000 1.2277 0.0000 0.93693






Table 2: Tab. 2. Plane and scalar irradiances for a collimated incident beam and no scattering within the water.

A run was then done with a heavily overcast sky to generate a diffuse sky radiance pattern with the sun’s location not discernable. The wind speed was 10ms1 to generate a non-level sea surface. The resulting irradiances are shown in Table 3.







location EouEodEuEd





in air 0.18863 1.7764 0.050456 1.0000





in water at depth 00.00000 1.1430 0.0000 0.94954






Table 3: Tab. 3. Plane and scalar irradiances for a diffuse incident sky radiance and no scattering within the water.

As before, these plane irradiances satisfy Eq. (3). However, the scalar irradiances do not satisfy Eq. (5). The reason is that Eq. (5) must be applied for each particular incident direction 𝜃i of the diffuse sky radiance, in order to correctly compute the angle factor seen in Eq. (5). If this is done one direction at a time (with the sun in a black sky), each individual incident direction satisfies Eq. (5) just as in the previous example. Thus energy in conserved across the surface ”beam by beam,” hence in toto, even if it is not obvious from the total scalar irradiances.

A further complication occurs when the water body has scattering. To illustrate this, the scattering coefficient was set to b = 0.4m1 and an ”average-particle” phase function was used in the previous simulation. The computed irradiance were then







location EouEodEuEd





in air 0.21264 1.7764 0.062372 1.0000





in water at depth 00.07922 1.2046 0.031115 0.96873






Table 4: Tab 4: Plane and scalar irradiances for a diffuse incident radiance, with scattering in the water.

Now even the plane irradiance appears to violate conservation of energy, Eq. (3). The reason is that Eou and Eu in air contain both surface-reflected radiance (as before) and radiance transmitted upward through the sea surface. Likewise, Eod and Ed in the water contain both downward transmitted irradiance (as before) as well as upwelling radiance that has been reflected back downward by the surface. This makes it appear at first glance that the irradiances do not add up correctly, even though energy actually is conserved across the air-water surface. The effects of both the surface itself and the water body can be accounted for simply by tallying the plane irradiances incident onto and leaving the surface from above and below:

Ed(downwelling,inair) Eu(upwelling,inair) = Ed(downwelling,inwater) Eu(upwelling,inwater). (6)

Equation (6) expresses conservation of energy for the surface plus water body, for any conditions of incident lighting and water IOPs. The irradiances seen in Table 4 satisfy this equation.

Conservation in terms of radiance

Another complication occurs when expressing conservation of energy across the surface in terms of radiance. Now it is necessary to account for changes in both the beam cross sectional area and in solid angle when going across the surface. When interpreting HydroLight output, it must be remembered that the computed radiances are averages over ”quads” or solid angles of finite size, as discussed on the HydroLight page. Such quads are represented by the green areas in Fig. 2.


PIC

Figure 2: Fig. 2. Illustration of the HydroLight radiance quads as needed to express energy conservation for a collimated beam across a level sea surface.

Remembering that radiance is power per unit area per unit solid angle, Eq. (2) can be written as

LiAiΔΩi = LrArΔΩr + LtAtΔΩt,

or

Li = Lr + Lt AtΔΩt Ai,ΔΩi,

after noting that Ar = Ai and ΔΩr = ΔΩi by the law of reflection. As noted before, AtAi = cos𝜃tcos𝜃i. The solid angles are given by ΔΩ = Δ(cos𝜃)Δϕ, where the angle ranges are determined by the 𝜃 and ϕ boundaries of the quads. Thus the last equation becomes

Li = Lr + Lt cos𝜃t cos𝜃iΔ(cos𝜃t) Δ(cos𝜃i), (7)

since Δϕt = Δϕi for the HydroLight quad layout. These angle factors must be evaluated for the particular quads associated with the incident and transmitted beams.

Consider again the previous case of the sun in a black sky at 𝜃i = 60deg, a level water surface, and no scattering. The incident and reflected HydroLight quads are centered at 60 deg and extend from 55 to 65 deg. Snell’s law gives the transmitted direction as 𝜃t = sin1[(sin𝜃i)n] = 40.26deg. Thus the transmitted radiance is contained in the HydroLight quad centered at 40 deg and extending from 35 to 45 deg. For the transmitted quad, for example, Δ(cos𝜃t) = cos35 cos45 = 0.11205. Evaluating the angle factors in Eq. (7) for these quads gives

Li = Lr + Lt0.76604 0.500000.11205 0.15096. (8)

The corresponding computed quad-averaged radiances for this run were Li = 50.7996, Lr = 3.21094, and Lt = 41.8544Wm2sr1nm1. These radiances satisfy Eq. (8). Thus energy expressed as radiance is conserved beam-by-beam across the water surface.

We have seen that conservation of energy across the sea surface can be expressed in various ways in terms of radiance and irradiance. However, those expressions are often written for collimated incident beams and consider only the surface itself (Eqs. 3, 5, and 7). It is therefore not always obvious that energy is conserved for the entire surface plus water column when looking at data or simulations for realistic conditions of sky radiances and water IOPs. In general, Eq. (6) should be used to check conservation of energy across the sea surface with measured or modeled plane irradiances.

When making radiance or irradiance measurements in the ocean, it is sometimes hard to verify that energy is being conserved. This is equally true when looking at the output from a numerical model such as HydroLight. Confusion most often arises when comparing measurements made just above and below the sea surface and observing that the measured (or predicted) radiances do not seem to ”add up” correctly. To resolve such confusion, first note that it’s the Law of Conservation of Energy, not the law of conservation of radiance or irradiance. We must therefore express the law of conservation of energy in terms of radiance or irradiance as appropriate to the measurements being made.

Within the Water

Within the water column, if there are no internal sources such as bioluminescence or inelastic scatter contributing to the wavelength of interest, conservation of energy is expressed in terms of irradiances by Gershun’s law:

a(z,λ) = 1 Eo(z,λ) d[Ed(z,λ) Eu(z,λ)] dz . (1)

Here a is the absorption coefficient, Eo is the scalar irradiance, and Ed and Eu are the downwelling and upwelling plane irradiances. This equation can be illustrated using numerical results generated by HydroLight. A run was made with the sun placed at a 60 deg zenith angle in a clear sky; the wind speed was 5ms1, and the water was infinitely deep. The absorption coefficient was set to a = 0.1m1, the scattering coefficient to b = 0.4m1, and an ”average-particle” phase function was chosen. (The run used HydroLight’s ”abconst” IOP model for these inputs.) No internal sources were included in the run. Table 1 shows the computed irradiances at depths of 5.00 and 5.01 m. Closely spaced depths are used to illustrate Eq. (1) so that the depth derivative can be accurately approximated as a finite difference and the scalar irradiance can be taken as the average of the values at 5.00 and 5.01 m.






depth (m)EoEuEd




5.00 0.51833 0.013151 0.32613




5.01 0.51749 0.013129 0.32559





Table 1: Tab. 1. Irradiances computed within the water body as described in the text. Irradiances have units of Wm2nm1.

Using these values in the finite difference approximation of Eq. (1) gives

a = 1 0.5(0.51833 + 0.51749)(0.32559 0.013129) (0.32613 0.013151) 5.01 5.00 = 0.1000m1.

The absorption coefficient as computed from the irradiances via Gershun’s law is the same as the one used as input to the run, so HydroLight is conserving energy in its in-water solution of the radiative transfer equation. (HydroLight also conserves energy if internal sources are present. Demonstration of that requires adding an appropriate source term to Gershun’s equation; see Light and Water (1994) Eq. 5.34.) Such accuracy cannot be expected with real data because of imperfect instrument calibration and other sources of error such as Raman scatter (an internal source not accounted for in Eq. 1), which will always be present to some degree during daylight measurements. Nevertheless, Gershun’s law can be a useful way to retrieve absorption coefficients from in-water radiance or irradiance measurements, as seen in papers by Voss (1989) and Maffione et al. (1993).

Across the Air-Water Surface

The situation is more complicated when considering energy conservation across the air-water surface. Consider a collimated beam of light incident onto a level sea surface. Part will be reflected and part will be transmitted into the water. Figure 1 shows this geometry and various quantities needed to express conservation of energy at the surface.


PIC

Figure 1: Fig. 1. Geometry needed for expressing the law of conservation of energy in terms of irradiances across a level sea surface.

Conservation of energy (or equivalently, power) across the surface requires that

Pi = Pr + Pt, (2)

where Pi is the power in an incident collimated beam of cross section Ai, Pr is the power in the reflected beam of cross section Ar, and Pt is the power in transmitted beam of cross section At. These beam cross sectional areas are shown in green in Fig. 1. The beam of incident power illuminates a horizontal area As of the level sea surface (shown in blue).

Conservation in terms of plane irradiances

Conservation of energy can be expressed in terms of incident (downwelling), reflected (upwelling), and transmitted (downwelling) plane irradiances using the horizontal projections of the beam cross section areas. Recalling that plane irradiance is power per unit horizontal area, Eq. (2) becomes

ApEd(incident,inair) = ApEu(reflected,inair) + ApEd(transmitted,inwater),

where the horizontally projected areas Ap corresponding to each beam are shown in yellow in Fig. 1. Since each beam has the same horizontally projected area, this equation reduces to just

Ed(incident,inair) = Eu(reflected,inair) + Ed(transmitted,inwater). (3)

Equation (3) is conservation of energy across the surface expressed in terms of plane irradiances for a collimated incident beam.

Conservation in terms of scalar irradiances

To express Eq. (2) in terms of the scalar irradiances, first recall how Eod is obtained from the radiance (Eq 5 of the Geometrical Radiometry page):

Eod = 2πdL(ξ̂)dΩ(ξ̂).

For a collimated incident beam in direction ξo ̂, we can write the radiance in terms of the beam irradiance and a Dirac delta function to get

Eod = 2πdEδ(ξ̂ ξ o ̂)dΩ(ξ̂) = E ,

where E is the incident irradiance on the beam cross sectional area; E = PiAi. Similar equations hold for the reflected and transmitted scalar irradiances. These beam cross sectional areas are shown in green in Fig. 1. Thus Eq. (2) becomes

AiEod(incident,inair) = ArEou(reflected,inair) + AtEod(transmitted,inwater),

or

Eod(incident,inair) = Eou(reflected,inair) + AtEod(transmitted,inwater)At Ai, (4)

after noting that Ar = Ai by the law of reflection. By geometry, the ratio of areas AtAi is just cos𝜃tcos𝜃i. 𝜃t can be written in terms of 𝜃i using Snell’s law, sin𝜃i = nsin𝜃t, where n is the real index of refraction of the water. Equation (4) then becomes

Eod(incident,inair) = Eou(reflected,inair) + Eod(transmitted,inwater) 1 cos𝜃i1 sin 2 𝜃i n2 . (5) 

Equation (5) is conservation of energy expressed in terms of scalar irradiance for a collimated incident beam.

To illustrate Equations (3) and (5) with HydroLight output, a run was made with the sun at a zenith angle of 𝜃i = 60deg in a black sky, in order to obtain a collimated incident beam. The incident Ed onto the surface was set to 1. The sea surface was level (zero wind speed), and the water index of refraction was n = 1.34. The scattering coefficient within in the water was set to zero, so that upwelling light from the water column would not confuse the illustration of energy conservation across the sea surface itself. The absorption coefficient was set to a = 0.1m1. (These runs used HydroLight IOP model ”abconst” and the ”idealized sky model”).

The computed irradiances just above and below the surface are shown in Table 2. The upwelling irradiances in the water are zero because there was no scattering by the water and the bottom was infinitely deep. These computed irradiances satisfy Equations (3) and (5), showing that HydroLight conserves energy across the surface.







location EouEodEuEd





in air 0.12690 2.0077 0.063209 1.0000





in water at depth 00.00000 1.2277 0.0000 0.93693






Table 2: Tab. 2. Plane and scalar irradiances for a collimated incident beam and no scattering within the water.

A run was then done with a heavily overcast sky to generate a diffuse sky radiance pattern with the sun’s location not discernable. The wind speed was 10ms1 to generate a non-level sea surface. The resulting irradiances are shown in Table 3.







location EouEodEuEd





in air 0.18863 1.7764 0.050456 1.0000





in water at depth 00.00000 1.1430 0.0000 0.94954






Table 3: Tab. 3. Plane and scalar irradiances for a diffuse incident sky radiance and no scattering within the water.

As before, these plane irradiances satisfy Eq. (3). However, the scalar irradiances do not satisfy Eq. (5). The reason is that Eq. (5) must be applied for each particular incident direction 𝜃i of the diffuse sky radiance, in order to correctly compute the angle factor seen in Eq. (5). If this is done one direction at a time (with the sun in a black sky), each individual incident direction satisfies Eq. (5) just as in the previous example. Thus energy in conserved across the surface ”beam by beam,” hence in toto, even if it is not obvious from the total scalar irradiances.

A further complication occurs when the water body has scattering. To illustrate this, the scattering coefficient was set to b = 0.4m1 and an ”average-particle” phase function was used in the previous simulation. The computed irradiance were then







location EouEodEuEd





in air 0.21264 1.7764 0.062372 1.0000





in water at depth 00.07922 1.2046 0.031115 0.96873






Table 4: Tab 4: Plane and scalar irradiances for a diffuse incident radiance, with scattering in the water.

Now even the plane irradiance appears to violate conservation of energy, Eq. (3). The reason is that Eou and Eu in air contain both surface-reflected radiance (as before) and radiance transmitted upward through the sea surface. Likewise, Eod and Ed in the water contain both downward transmitted irradiance (as before) as well as upwelling radiance that has been reflected back downward by the surface. This makes it appear at first glance that the irradiances do not add up correctly, even though energy actually is conserved across the air-water surface. The effects of both the surface itself and the water body can be accounted for simply by tallying the plane irradiances incident onto and leaving the surface from above and below:

Ed(downwelling,inair) Eu(upwelling,inair) = Ed(downwelling,inwater) Eu(upwelling,inwater). (6)

Equation (6) expresses conservation of energy for the surface plus water body, for any conditions of incident lighting and water IOPs. The irradiances seen in Table 4 satisfy this equation.

Conservation in terms of radiance

Another complication occurs when expressing conservation of energy across the surface in terms of radiance. Now it is necessary to account for changes in both the beam cross sectional area and in solid angle when going across the surface. When interpreting HydroLight output, it must be remembered that the computed radiances are averages over ”quads” or solid angles of finite size, as discussed on the HydroLight page. Such quads are represented by the green areas in Fig. 2.


PIC

Figure 2: Fig. 2. Illustration of the HydroLight radiance quads as needed to express energy conservation for a collimated beam across a level sea surface.

Remembering that radiance is power per unit area per unit solid angle, Eq. (2) can be written as

LiAiΔΩi = LrArΔΩr + LtAtΔΩt,

or

Li = Lr + Lt AtΔΩt Ai,ΔΩi,

after noting that Ar = Ai and ΔΩr = ΔΩi by the law of reflection. As noted before, AtAi = cos𝜃tcos𝜃i. The solid angles are given by ΔΩ = Δ(cos𝜃)Δϕ, where the angle ranges are determined by the 𝜃 and ϕ boundaries of the quads. Thus the last equation becomes

Li = Lr + Lt cos𝜃t cos𝜃iΔ(cos𝜃t) Δ(cos𝜃i), (7)

since Δϕt = Δϕi for the HydroLight quad layout. These angle factors must be evaluated for the particular quads associated with the incident and transmitted beams.

Consider again the previous case of the sun in a black sky at 𝜃i = 60deg, a level water surface, and no scattering. The incident and reflected HydroLight quads are centered at 60 deg and extend from 55 to 65 deg. Snell’s law gives the transmitted direction as 𝜃t = sin1[(sin𝜃i)n] = 40.26deg. Thus the transmitted radiance is contained in the HydroLight quad centered at 40 deg and extending from 35 to 45 deg. For the transmitted quad, for example, Δ(cos𝜃t) = cos35 cos45 = 0.11205. Evaluating the angle factors in Eq. (7) for these quads gives

Li = Lr + Lt0.76604 0.500000.11205 0.15096. (8)

The corresponding computed quad-averaged radiances for this run were Li = 50.7996, Lr = 3.21094, and Lt = 41.8544Wm2sr1nm1. These radiances satisfy Eq. (8). Thus energy expressed as radiance is conserved beam-by-beam across the water surface.

We have seen that conservation of energy across the sea surface can be expressed in various ways in terms of radiance and irradiance. However, those expressions are often written for collimated incident beams and consider only the surface itself (Eqs. 3, 5, and 7). It is therefore not always obvious that energy is conserved for the entire surface plus water column when looking at data or simulations for realistic conditions of sky radiances and water IOPs. In general, Eq. (6) should be used to check conservation of energy across the sea surface with measured or modeled plane irradiances.

When making radiance or irradiance measurements in the ocean, it is sometimes hard to verify that energy is being conserved. This is equally true when looking at the output from a numerical model such as HydroLight. Confusion most often arises when comparing measurements made just above and below the sea surface and observing that the measured (or predicted) radiances do not seem to ”add up” correctly. To resolve such confusion, first note that it’s the Law of Conservation of Energy, not the law of conservation of radiance or irradiance. We must therefore express the law of conservation of energy in terms of radiance or irradiance as appropriate to the measurements being made.

Within the Water

Within the water column, if there are no internal sources such as bioluminescence or inelastic scatter contributing to the wavelength of interest, conservation of energy is expressed in terms of irradiances by Gershun’s law:

a(z,λ) = 1 Eo(z,λ) d[Ed(z,λ) Eu(z,λ)] dz . (1)

Here a is the absorption coefficient, Eo is the scalar irradiance, and Ed and Eu are the downwelling and upwelling plane irradiances. This equation can be illustrated using numerical results generated by HydroLight. A run was made with the sun placed at a 60 deg zenith angle in a clear sky; the wind speed was 5ms1, and the water was infinitely deep. The absorption coefficient was set to a = 0.1m1, the scattering coefficient to b = 0.4m1, and an ”average-particle” phase function was chosen. (The run used HydroLight’s ”abconst” IOP model for these inputs.) No internal sources were included in the run. Table 1 shows the computed irradiances at depths of 5.00 and 5.01 m. Closely spaced depths are used to illustrate Eq. (1) so that the depth derivative can be accurately approximated as a finite difference and the scalar irradiance can be taken as the average of the values at 5.00 and 5.01 m.






depth (m)EoEuEd




5.00 0.51833 0.013151 0.32613




5.01 0.51749 0.013129 0.32559





Table 1: Tab. 1. Irradiances computed within the water body as described in the text. Irradiances have units of Wm2nm1.

Using these values in the finite difference approximation of Eq. (1) gives

a = 1 0.5(0.51833 + 0.51749)(0.32559 0.013129) (0.32613 0.013151) 5.01 5.00 = 0.1000m1.

The absorption coefficient as computed from the irradiances via Gershun’s law is the same as the one used as input to the run, so HydroLight is conserving energy in its in-water solution of the radiative transfer equation. (HydroLight also conserves energy if internal sources are present. Demonstration of that requires adding an appropriate source term to Gershun’s equation; see Light and Water (1994) Eq. 5.34.) Such accuracy cannot be expected with real data because of imperfect instrument calibration and other sources of error such as Raman scatter (an internal source not accounted for in Eq. 1), which will always be present to some degree during daylight measurements. Nevertheless, Gershun’s law can be a useful way to retrieve absorption coefficients from in-water radiance or irradiance measurements, as seen in papers by Voss (1989) and Maffione et al. (1993).

Across the Air-Water Surface

The situation is more complicated when considering energy conservation across the air-water surface. Consider a collimated beam of light incident onto a level sea surface. Part will be reflected and part will be transmitted into the water. Figure 1 shows this geometry and various quantities needed to express conservation of energy at the surface.


PIC

Figure 1: Fig. 1. Geometry needed for expressing the law of conservation of energy in terms of irradiances across a level sea surface.

Conservation of energy (or equivalently, power) across the surface requires that

Pi = Pr + Pt, (2)

where Pi is the power in an incident collimated beam of cross section Ai, Pr is the power in the reflected beam of cross section Ar, and Pt is the power in transmitted beam of cross section At. These beam cross sectional areas are shown in green in Fig. 1. The beam of incident power illuminates a horizontal area As of the level sea surface (shown in blue).

Conservation in terms of plane irradiances

Conservation of energy can be expressed in terms of incident (downwelling), reflected (upwelling), and transmitted (downwelling) plane irradiances using the horizontal projections of the beam cross section areas. Recalling that plane irradiance is power per unit horizontal area, Eq. (2) becomes

ApEd(incident,inair) = ApEu(reflected,inair) + ApEd(transmitted,inwater),

where the horizontally projected areas Ap corresponding to each beam are shown in yellow in Fig. 1. Since each beam has the same horizontally projected area, this equation reduces to just

Ed(incident,inair) = Eu(reflected,inair) + Ed(transmitted,inwater). (3)

Equation (3) is conservation of energy across the surface expressed in terms of plane irradiances for a collimated incident beam.

Conservation in terms of scalar irradiances

To express Eq. (2) in terms of the scalar irradiances, first recall how Eod is obtained from the radiance (Eq 5 of the Geometrical Radiometry page):

Eod = 2πdL(ξ̂)dΩ(ξ̂).

For a collimated incident beam in direction ξo ̂, we can write the radiance in terms of the beam irradiance and a Dirac delta function to get

Eod = 2πdEδ(ξ̂ ξ o ̂)dΩ(ξ̂) = E ,

where E is the incident irradiance on the beam cross sectional area; E = PiAi. Similar equations hold for the reflected and transmitted scalar irradiances. These beam cross sectional areas are shown in green in Fig. 1. Thus Eq. (2) becomes

AiEod(incident,inair) = ArEou(reflected,inair) + AtEod(transmitted,inwater),

or

Eod(incident,inair) = Eou(reflected,inair) + AtEod(transmitted,inwater)At Ai, (4)

after noting that Ar = Ai by the law of reflection. By geometry, the ratio of areas AtAi is just cos𝜃tcos𝜃i. 𝜃t can be written in terms of 𝜃i using Snell’s law, sin𝜃i = nsin𝜃t, where n is the real index of refraction of the water. Equation (4) then becomes

Eod(incident,inair) = Eou(reflected,inair) + Eod(transmitted,inwater) 1 cos𝜃i1 sin 2 𝜃i n2 . (5) 

Equation (5) is conservation of energy expressed in terms of scalar irradiance for a collimated incident beam.

To illustrate Equations (3) and (5) with HydroLight output, a run was made with the sun at a zenith angle of 𝜃i = 60deg in a black sky, in order to obtain a collimated incident beam. The incident Ed onto the surface was set to 1. The sea surface was level (zero wind speed), and the water index of refraction was n = 1.34. The scattering coefficient within in the water was set to zero, so that upwelling light from the water column would not confuse the illustration of energy conservation across the sea surface itself. The absorption coefficient was set to a = 0.1m1. (These runs used HydroLight IOP model ”abconst” and the ”idealized sky model”).

The computed irradiances just above and below the surface are shown in Table 2. The upwelling irradiances in the water are zero because there was no scattering by the water and the bottom was infinitely deep. These computed irradiances satisfy Equations (3) and (5), showing that HydroLight conserves energy across the surface.







location EouEodEuEd





in air 0.12690 2.0077 0.063209 1.0000





in water at depth 00.00000 1.2277 0.0000 0.93693






Table 2: Tab. 2. Plane and scalar irradiances for a collimated incident beam and no scattering within the water.

A run was then done with a heavily overcast sky to generate a diffuse sky radiance pattern with the sun’s location not discernable. The wind speed was 10ms1 to generate a non-level sea surface. The resulting irradiances are shown in Table 3.







location EouEodEuEd





in air 0.18863 1.7764 0.050456 1.0000





in water at depth 00.00000 1.1430 0.0000 0.94954






Table 3: Tab. 3. Plane and scalar irradiances for a diffuse incident sky radiance and no scattering within the water.

As before, these plane irradiances satisfy Eq. (3). However, the scalar irradiances do not satisfy Eq. (5). The reason is that Eq. (5) must be applied for each particular incident direction 𝜃i of the diffuse sky radiance, in order to correctly compute the angle factor seen in Eq. (5). If this is done one direction at a time (with the sun in a black sky), each individual incident direction satisfies Eq. (5) just as in the previous example. Thus energy in conserved across the surface ”beam by beam,” hence in toto, even if it is not obvious from the total scalar irradiances.

A further complication occurs when the water body has scattering. To illustrate this, the scattering coefficient was set to b = 0.4m1 and an ”average-particle” phase function was used in the previous simulation. The computed irradiance were then







location EouEodEuEd





in air 0.21264 1.7764 0.062372 1.0000





in water at depth 00.07922 1.2046 0.031115 0.96873






Table 4: Tab 4: Plane and scalar irradiances for a diffuse incident radiance, with scattering in the water.

Now even the plane irradiance appears to violate conservation of energy, Eq. (3). The reason is that Eou and Eu in air contain both surface-reflected radiance (as before) and radiance transmitted upward through the sea surface. Likewise, Eod and Ed in the water contain both downward transmitted irradiance (as before) as well as upwelling radiance that has been reflected back downward by the surface. This makes it appear at first glance that the irradiances do not add up correctly, even though energy actually is conserved across the air-water surface. The effects of both the surface itself and the water body can be accounted for simply by tallying the plane irradiances incident onto and leaving the surface from above and below:

Ed(downwelling,inair) Eu(upwelling,inair) = Ed(downwelling,inwater) Eu(upwelling,inwater). (6)

Equation (6) expresses conservation of energy for the surface plus water body, for any conditions of incident lighting and water IOPs. The irradiances seen in Table 4 satisfy this equation.

Conservation in terms of radiance

Another complication occurs when expressing conservation of energy across the surface in terms of radiance. Now it is necessary to account for changes in both the beam cross sectional area and in solid angle when going across the surface. When interpreting HydroLight output, it must be remembered that the computed radiances are averages over ”quads” or solid angles of finite size, as discussed on the HydroLight page. Such quads are represented by the green areas in Fig. 2.


PIC

Figure 2: Fig. 2. Illustration of the HydroLight radiance quads as needed to express energy conservation for a collimated beam across a level sea surface.

Remembering that radiance is power per unit area per unit solid angle, Eq. (2) can be written as

LiAiΔΩi = LrArΔΩr + LtAtΔΩt,

or

Li = Lr + Lt AtΔΩt Ai,ΔΩi,

after noting that Ar = Ai and ΔΩr = ΔΩi by the law of reflection. As noted before, AtAi = cos𝜃tcos𝜃i. The solid angles are given by ΔΩ = Δ(cos𝜃)Δϕ, where the angle ranges are determined by the 𝜃 and ϕ boundaries of the quads. Thus the last equation becomes

Li = Lr + Lt cos𝜃t cos𝜃iΔ(cos𝜃t) Δ(cos𝜃i), (7)

since Δϕt = Δϕi for the HydroLight quad layout. These angle factors must be evaluated for the particular quads associated with the incident and transmitted beams.

Consider again the previous case of the sun in a black sky at 𝜃i = 60deg, a level water surface, and no scattering. The incident and reflected HydroLight quads are centered at 60 deg and extend from 55 to 65 deg. Snell’s law gives the transmitted direction as 𝜃t = sin1[(sin𝜃i)n] = 40.26deg. Thus the transmitted radiance is contained in the HydroLight quad centered at 40 deg and extending from 35 to 45 deg. For the transmitted quad, for example, Δ(cos𝜃t) = cos35 cos45 = 0.11205. Evaluating the angle factors in Eq. (7) for these quads gives

Li = Lr + Lt0.76604 0.500000.11205 0.15096. (8)

The corresponding computed quad-averaged radiances for this run were Li = 50.7996, Lr = 3.21094, and Lt = 41.8544Wm2sr1nm1. These radiances satisfy Eq. (8). Thus energy expressed as radiance is conserved beam-by-beam across the water surface.

We have seen that conservation of energy across the sea surface can be expressed in various ways in terms of radiance and irradiance. However, those expressions are often written for collimated incident beams and consider only the surface itself (Eqs. 3, 5, and 7). It is therefore not always obvious that energy is conserved for the entire surface plus water column when looking at data or simulations for realistic conditions of sky radiances and water IOPs. In general, Eq. (6) should be used to check conservation of energy across the sea surface with measured or modeled plane irradiances.

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