Abstract The remote sensing reflectance R rs , concentrations of chlorophyll a and other pigments C i , suspended particulate matter concentrations C SPM and coloured dissolved organic matter absorption coefficient a CDOM (λ) were measured in the euphotic zones of 15 Pomeranian lakes in 2007–2010. On the basis of 235 sets of data points obtained from simultaneous estimates of these quantities, we classified the lake waters into three types. The first one, with the lowest a CDOM (440 nm) (usually between 0.1 and 1.3 m −1 and chlorophyll a concentrations 1.3 C a −3 ), displays a broad peak on the reflectance spectrum at 560–580 nm and resembles the shape of the remote sensing reflectance spectra usually observed in the Baltic Proper. A set of R rs spectra from the Baltic Proper is given for comparison. The second lake water type has a very high CDOM absorption coefficient (usually a CDOM (440 nm) > 10 m −1 , up to 17.4 m −1 in Lake Pyszne; it has a relatively low reflectance ( R rs −1 ) over the entire spectral range, and two visible reflectance spectra peaks at ca 650 and 690–710 nm. The third type of lake water represents waters with a lower CDOM absorption coefficient (usually a CDOM (440 nm) −1 ) and a high chlorophyll a concentration (usually C a > 4 mg m −3 , up to 336 mg m −3 in Lake Gardno). The remote sensing reflectance spectra in these waters always exhibit three peaks ( R rs > 0.005 sr −1 ): a broad one at 560–580 nm, a smaller one at ca 650 nm and a well-pronounced one at 690–720 nm. These R rs (λ) peaks correspond to the relatively low absorption of light by the various optically active components of the lake water and the considerable scattering (over the entire spectral range investigated) due to the high SPM concentrations there. The remote sensing maximum at λ ≈ 690–720 nm is higher still as a result of the natural fluorescence of chlorophyll a . Empirical relationships between the spectral reflectance band ratios at selected wavelengths and the various optically active components for these lake waters are also established: for example, the chlorophyll a concentration in surface water layer C a = 6.432 e 4.556 X , where X = [max R rs (695 ≤ λ ≤ 720) – R rs (λ = 670)]/max R rs (695 ≤ λ ≤ 720), and the coefficient of determination R 2 = 0.95.
[1]
Howard R. Gordon,et al.
Remote Assessment of Ocean Color for Interpretation of Satellite Visible Imagery
,
1983,
Lecture Notes on Coastal and Estuarine Studies.
[2]
James W. Brown,et al.
A semianalytic radiance model of ocean color
,
1988
.
[3]
B. Mitchell,et al.
Variability in pigment particulate fluorescence and absorption spectra in the northeastern Pacific Ocean
,
1988
.
[4]
P. Kowalczuk,et al.
Validation of empirical and semi-analytical remote sensing algorithms for estimating absorption by Coloured Dissolved Organic Matter in the Baltic Sea from SeaWiFS and MODIS imagery
,
2010
.
[5]
P. Kowalczuk,et al.
Optical characteristics of two contrasting Case 2 waters and their influence on remote sensing algorithms
,
2003
.
[6]
B. Woźniak,et al.
Light absorption in sea water
,
2007
.
[7]
M. Darecki,et al.
SeaWiFS ocean colour chlorophyll algorithms for the southern Baltic Sea
,
2005
.
[8]
Anatoly A. Gitelson,et al.
Remote chlorophyll-a retrieval in turbid, productive estuaries : Chesapeake Bay case study
,
2007
.
[9]
Mirosław Darecki,et al.
Algorithms for the remote sensing of the Baltic ecosystem (DESAMBEM). Part 2: Empirical validation
,
2008
.
[10]
H. Gordon,et al.
Remote Assessment of Ocean Color for Interpretation of Satellite Visible Imagery: A Review
,
1983
.
[11]
R. W. Austin,et al.
SeaWiFS technical report series. Volume 25: Ocean optics protocols for SeaWiFS validation, revision 1
,
1995
.