Page updated: March 13, 2021
Author: Collin Roesler
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Non-Algal Particles (NAP)

As noted in the introduction to this chapter, the term non-algal particles (NAPs) refers to particulate matter that does not have extractable (via solvents such as acetone or methanol) pigments. This includes all living and detrital organic matter such as the non-pigmented portion of phytoplankton cells, detritus, heterotrophic bacteria, and viruses. Many authors also include inorganic mineral particles of both biogenic (e.g., calcite liths and shells) and terrestrial origin (e.g., clay, silt, and sand).


Detritus is a catch-all term for non-living particulate organic matter, including dead bacterial, phytoplankton and zooplankton cells, fragments of cells left from zooplankton grazing, fecal pellets, shells, and marine snow aggregates. Detritus both absorbs and scatters and can constitute an important fraction of the total IOPs of a water body.

Absorption by detritus

There have been many measurements of the absorption spectra of detritus and NAPs. Figure 1 shows an example. These measurements include both biogenic detritus and whatever mineral particles (if any) were in the water. Although magnitudes vary greatly depending on the concentration of NAPs in the water, the curves show a generally exponential decay with increasing wavelength. It is thus common (Kirk (1980), Roesler et al. (1989), Bricaud et al. (1998)) to model absorption by detritus or NAPs via

aNAP(λ) = aNAP(λo) exp SNAP(λλo)[m1], (1)

where λo is a reference wavelength and SNAP the spectral slope parameter. The mean value of SNAP used to model NAP absorption is 0.011nm1 (e.g., Roesler et al. (1989), Bricaud et al. (1998)). However, as always with data-derived parameters, there is variability in SNAP. Figure 2 shows the distribution of SNAP values observed by Babin et al. (2003b). Their data show a mean of SNAP = 0.0123nm1 with a standard deviation of 0.0013.


Figure 1: Measurements of detritus absorption spectra from the Sargasso Sea. Redrawn from Bricaud and Stramski (1990) [reproduction approval pending].


Figure 2: Distribution of SNAP measured on 348 samples in European waters. Figure 14(a) of Babin et al. (2003b), reproduced by permission of the American Geophysical Union.

The absorption model of Eq. (1) has the same functional form as that for absorption by CDOM, although the average spectral slope parameter SNAP 0.011nm1 differs somewhat from the average parameter for CDOM, SCDOM 0.018nm1; see Commonly Used Models for IOPs and Biogeochemistry.

Scattering by detritus

Although CDOM and NAPs have similar absorption spectra, they differ greatly in their scattering properties: CDOM has negligible scattering, but NAPs can be strongly scattering. There is much less data on NAP scattering than for absorption, but Fig. 3 shows data from Great Lake (Taihu), China. The bNAP(λ) spectra in this dataset show a rather featureless dependence on wavelength, which is well fit (R2 = 0.989) by a power law:

bNAP(λ) = bNAP(550) λ 550 0.938[m1]. (2)

The authors show that the IOPs of this lake are dominated by NAP, with phytoplankton usually contributing less that 10% of the total scattering. (The same dataset had NAP absorption spectra that were well fit by Eq. (1), but with a spectral slope parameter of SNAP = 0.0052 ± 0.0010nm1, which is about one-half of typical ocean values.)


Figure 3: Scattering coefficient spectra bNAP(λ) from Great Lake (Taihu), China. Data from Fig. 1(B) of Sun et al. (2010) provided courtesy of D. Sun.


Mineral particles can enter the ocean from river discharge, erosion of coastal cliffs, sediment resuspension, and deposition of atmosphere dust, which is often carried long distances by winds. The optical properties of such particles are just as varied, and often just as important, as the properties of biological particles. In spite of their importance, relatively few studies have investigated the absorption and scattering properties of minerals per se. These include Ahn (1999), Stramski et al. (2004), Babin and Stramski (2004), and Stramski et al. (2007).

Absorption by minerals

Figure 4 shows mass-specific absorption coefficients a(λ) (units of m2g1) for four types of minerals. Figure 5 shows the same for several types of mineral dust suspended in sea water; some of the curves are the same mineral type but with different particle size distributions. The imaginary indices of refraction for these particles varied by an order of magnitude, from about 0.003 to 0.03, depending on wavelength and mineral type. See Stramski et al. (2007) for a full discussion. These (and other) data sets are in qualitative agreement: absorption by minerals can range from highly absorbing in the blue with a roughly exponential decrease with increasing wavelength, to almost non-absorbing and spectrally flat. Thus, to first order, absorption by minerals can be modeled by either an exponential,

amin(λ) = amin(λref) exp[Smin(λ λref)][m1],

or a power law,

amin(λ) = amin(λref) λ λref mmin [m1],

where λref is a reference wavelength. The parameters Smin and mmin can be adjusted as needed to fit a particular mineral type.


Figure 4: Measured mass-specific absorption coefficients a(λ) for four types of mineral. From Ahn (1999); data courtesy of A. Morel.


Figure 5: Measured mass-specific absorption coefficients a(λ) for various types of mineral dust suspended in sea water. The highest magnitude curves are red soils rich in iron oxides, the lowest curves are calcite and quartz. Redrawn from Fig. 3 of Stramski et al. (2007) with data provided courtesy of D. Stramski.

Scattering by minerals

Figures 6 and 7 show the mass-specific scattering coefficients b(λ) for the same two data sets of Figs. 4 and 5. As for absorption, the scattering coefficients show a decrease from blue to red, although with a couple of notable exceptions for the brown earth and Kosan samples, which have their maximum values at green wavelengths. Many of these scattering coefficients could be modeled with an exponential or power law function. However, in all cases, use of a measured spectrum for radiative transfer calculations is preferable.


Figure 6: Measured mass-specific scattering coefficients b(λ) for four types of minerals. From Ahn (1999); data courtesy of A. Morel.


Figure 7: Measured mass-specific scattering coefficients b(λ) for the same samples of mineral dust suspended in sea water as in Fig. 5. Redrawn from Fig. 6 of Stramski et al. (2007) with data provided courtesy of D. Stramski.

Stramski et al. (2001) used complex indices of refraction for detritus and mineral particles, a power law particle size distribution with a slope parameter of -4 (a Junge distribution), and Mie theory to compute absorption, scattering, and backscattering cross sections for detritus and minerals. Their results are shown in Table 1. It is interesting to note how closely the wavelength exponents for the scattering cross sections agree with the best-fit values for the NAP-dominated waters of Fig. 3 as seen in Eq. (2).

ComponentAbsorption Scattering Backscattering

Detritus σa, det = 8.79 × 1016e0.00847λσb, det = 1.43 × 1013λ0.9445σbb, det = 5.88 × 1016λ0.8997
Minerals σa, min = 1.01 × 1015e0.00846λσb, min = 7.71 × 1013λ0.9764σbb, min = 1.79 × 1014λ0.9140

Table 1: Absorption, scattering, and backscattering cross sections for detritus and minerals. All have units of m2 per particle. Multiplication by the number of particles per cubic meter gives a,b, and bb in units of m1. Data from Table 2 of Stramski et al. (2001).

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