Td corrigé Dynamic coastal processes can alter bio-optical properties, which ... pdf

Dynamic coastal processes can alter bio-optical properties, which ...

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Toward Closure of Upwelling Radiance in Coastal Waters
(To be submitted to Applied Optics: v4 3/26/02)

Grace C. Chang1, Emmanuel Boss2, Curtis D. Mobley3, Tommy D. Dickey1, and W. S. Pegau4

1Ocean Physics Laboratory, University of California at Santa Barbara, 6487 Calle Real Suite A, Santa Barbara, CA 93117, U.S.A.; grace.chang@opl.ucsb.edu

2University of Maine, School of Marine Sciences, 5741 Libby Hall, Orono, ME 04469, U.S.A.

3Sequoia Scientific, Inc., Westpark Technical Center, 15317 NE 90th St., Redmond, WA 98052, U.S.A.

4College of Oceanic and Atmospheric Sciences, Oregon State University, Corvallis, OR 97331, U.S.A.

Abstract
Upwelling radiance is an important quantity for interpretation of ocean color remote sensing data. We present three methods for deriving water-leaving radiance, Lw(lð), and remote sensing reflectance using a HyperTSRB, profiled spectroradiometers, and Hydrolight 4.1 simulations. Average agreement between HyperTSRB and spectroradiometric determinations of Lw(lð) was 26%, 13%, and 17% at blue, green, and red wavelengths, respectively. Comparisons of HyperTSRB (and spectroradiometric) Lw(lð) with Hydrolight simulations yielded percent differences of 17% (18%), 17% (18%), and 13% (20%) for blue, green, and red wavelengths. The differences in Lw(lð) could largely be accounted for were largely dependent onby uncertenties in measurements and instrument errors and model assumptions. We present techniques for converting upwelling radiance to Lw(lð).
OCIS Codes: 010.4450, 120.0280, 120.4640

1.0 Introduction

We show methods for deriving Lw(lð) and Rrs(lð) using a tethered radiometric buoy, profiled spectroradiometers, and radiative transfer model simulations with measured inherent optical properties as inputs. We aim to find closure between the two in situ measurement methods as well as with radiative transfer modeling in turbid coastal waters. Techniques for converting Lu(lð,z) to Lw(lð) are also presented.

Spectral radiance is one of the fundamental quantities of interest in the field of ocean optics (Kirk, 1989; Mobley, 1994). It is important for quantifying ocean color/remote sensing, water column visibility, and photosynthesis. Over the past few decades, algorithms and models to relate remote sensing measurements to in-water constituents have been developed (e.g., Garver et al., 1994; Tassan, 1994; Roesler and Perry, 1995; Gould and Arnone, 1998; O’Reilly et al., 1998; He et al., 2000). Ocean color remote sensing data have been used to estimate chlorophyll concentration, spectral backscattering coefficient, spectral absorption coefficient, and spectral absorption coefficient separated into phytoplankton, detrital, and gelbstoff constituents. Some of the current problems with derivation of pigment concentrations and in-water optical properties from ocean color remote sensing include the presence of clouds, atmospheric corrections (Gordon and Wang, 1994; Gordon et al., 1997; Chomko and Gordon, 1998; Hu et al., 2000), extrapolation of region-specific to global ocean color algorithms (particularly for coastal waters), and determination of the vertical structure of optical and biological characteristics (Gordon and McCluney, 1975). Recently, increasing research efforts have been focused on the use of remote sensing data to resolve vertical structures and detect subsurface features such as internal waves, sediment plumes, bottom type, and bathymetry (Gould and Arnone, 1998; Barnard et al., 2000; Frette et al., 2001; Weidemann et al., 2001; Dierssen et al., submitted manuscript).

Radiance, L(qð,fð,ðlð,ð ðz), is defined as the radiant flux at a specified point with units of W m-2 sr-1 nm-1. It is dependent on zenith angle, qð; azimuthal angle, fð; wavelength, lð;ð ðand depth, z, assuming plane-parallel geometry. The spectral shape and magnitude of radiance is dependent on the influx of solar radiation at the sea surface, sea surface characteristics, and the optical properties of the water column. Upwelling radiance, Lu(lð, z), is the radiance of an upwelling light field at qð = pð. Lu(lð, z) is used to compute the spectral radiance reflectance (units of sr-1),

the ratio of the upwelling radiance to the downwelling irradiance, Ed(lð,ðz). Irradiance is the vertical component of radiant flux per unit surface area per unit wavelength (units of W m-2 nm-1). Taken just above the sea surface, rrs(lð) is termed the remote sensing reflectance,

where Lw(lð) is water-leaving radiance and Ed(lð) is solar spectral irradiance, both quantities measured just above the sea surface (z = 0+).

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Acknowledgements
This work was supported by the Office of Naval Research Environmental Optics Program as part of the HyCODE program. We would also like to thank François Baratange for his help in data collection and processing.
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Figures

Figure 1. LEO-15 site map showing the measurements made during the HyCODE experiment between July 21 and 27, 2000. Depth contours are approximate.

Figure 2. HyperTSRB (solid lines) and OCP (circles) comparisons of Lu(lð,ð0.66m) at the SeaWiFS wavelengths for (a and b) July 21, 2000; 39.37°N, 74.21°W, (c and d) July 22, 2000; 39.46°N, 74.26°W, (e and f) July 24, 2000; 39.49°N, 74.23°W, and (g and h) July 27, 2000; 39.36°N, 74.13°W. Differences between the two methods, calculated by equation (5), are shown in the right-hand column.


Figure 3. Comparisons between HyperTSRB (solid lines) and OCP (circles) measured Lu(lð,ð0.66m) (left two columns) and Lw(lð) (right two columns) with Hydrolight-computed (dashed lines) upwelling radiances for (a-d) July 21, 2000; 39.37°N, 74.21°W, (e-h) July 22, 2000; 39.46°N, 74.26°W, (i-l) July 24, 2000; 39.41°N, 74.20°W, and (m and n) July 27, 2000; 39.34°N, 74.08°W. No OCP data were obtained on July 27, 2000, therefore only HyperTSRB and Hydrolight Lu(lð,ð0.66m) are compared; Hydrolight-derived Lw(lð) is plotted as the dash-dotted line. Differences between methods, calculated by equation (5), are also shown.

Figure 4. Rrs(lð), derived from HyperTSRB (solid lines) and OCP (circles) measurements and Hydrolight simulations (dashed lines) for (a and b) July 21, 2000; 39.37°N, 74.21°W, (c and d) July 22, 2000; 39.46°N, 74.26°W, (e and f) July 24, 2000; 39.41°N, 74.20°W, and (g) July 27, 2000; 39.34°N, 74.08°W. Again, no OCP data were obtained on July 27, 2000, therefore only Hydrolight Rrs(lð)ð ðis shown. Differences between the methods, calculated by equation (5), are shown in the right-hand column.

Figure 5. Rrs(lð) = Lu(lð,ð0.66m)/Ed(lð,0+m) (dashed line with crosses) compared with Rrs(lð) = Lw(lð,0+m)/Ed(lð,0+m) (solid line with symbols) for July 24, 2000; 39.41°N, 74.20°W. HyperTSRB data are shown in (a and b) and OCP data are illustrated in (c and d). Differences were computed using equation (5) and shown in the right-hand column.

Figure 6. Maximum (circles), minimum (pluses), and mean (triangles) of the conversion factor, Fg(lð), for (a) July 21, 2000, (b) July 22, 2000, (c) July 24, 2000, and (d) July 27, 2000; and (e) standard deviation and (f) variance of the conversion factor, Fg(lð), averaged over all days and locations and averaged over each sampling day. The legend for the standard deviation and variance plots is shown in (e). Tables

Table 1. Average percent differences computed using equation (5) and r2 values between HyperTSRB and OCP Lu(lð,ð0.66m).
lð412442490532555590682r2July 21d30.8825.7718.9112.2312.6410.6910.250.969July 2242.4839.5233.3024.0323.239.00025.370.967July 24a48.9246.5739.4228.9628.2216.4233.840.972July 24b30.9529.7822.789.2858.26814.8216.580.968July 24c32.9933.3929.3918.8918.104.06825.030.972July 24d23.7523.8120.1710.9910.5912.0214.380.969July 27c22.0718.7111.858.6337.17030.197.9600.929Average34.7432.3626.2016.9816.4212.9719.730.966
Table 2. Average percent differences computed using equation (5) and r2 values between HyperTSRB and OCP Lw(lð).
lð412442490532555590682r2July 21d31.79 25.9918.3311.0811.5613.1811.140.956July 2225.89 21.5714.4110.7010.2616.7112.330.955July 24a48.44 45.2336.2423.9322.4510.2632.750.948July 24b19.13 21.7519.619.5739.29213.2812.700.961July 24c39.80 37.3327.0611.429.4228.85524.800.932July 24d10.44 10.559.4036.1165.72925.704.9340.961July 27c20.98 17.268.5916.0335.66039.8815.160.876Average29.84 27.1720.5112.2911.7316.0616.670.947

Table 3. Average percent differences computed using equation (5) and r2 values between HyperTSRB and Hydrolight and OCP and Hydrolight (in parentheses) for Lu(lð,ð0.66m).
lð412442490532555590682r2July 21a22.49 19.984.69012.2118.3423.0717.310.963July 21b2.883 1.96412.4723.8529.4838.469.4430.960July 21c2.995 1.34410.2020.0925.5735.5716.860.963July 21d1.023
(30.65)2.327
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