A grid of polarization models for Rayleigh scattering planetary atmospheres^{}
E. Buenzli  H. M. Schmid
Institute for Astronomy, ETH Zurich, 8093 Zurich, Switzerland
Received 30 January 2009 / Accepted 27 June 2009
Abstract
Context. Reflected light from giant planets is polarized by scattering, offering the possibility of investigating atmospheric properties with polarimetry. Polarimetric measurements are available for the atmospheres of solar system planets, and instruments are being developed to detect and study the polarimetric properties of extrasolar planets.
Aims. We investigate the intensity and polarization of reflected light from planets in a systematic way with a grid of model calculations. Comparison of the results with existing and future observations can be used to constrain parameters of planetary atmospheres.
Methods. We present Monte Carlo simulations for planets with Rayleigh scattering atmospheres. We discuss the diskintegrated polarization for phase angles typical of extrasolar planet observations and for the limb polarization effect observable for solar system objects near opposition. The main parameters investigated are single scattering albedo, optical depth of the scattering layer, and albedo of an underlying Lambert surface for a homogeneous Rayleigh scattering atmosphere. We also investigate atmospheres with isotropic scattering and forward scattering aerosol particles, as well as models with two scattering layers.
Results. The reflected intensity and polarization depend strongly on the phase angle, as well as on atmospheric properties, such as the presence of absorbers or aerosol particles, column density of Rayleigh scattering particles and cloud albedo. Most likely to be detected are planets that produce a strong polarization flux signal because of an optically thick Rayleigh scattering layer. Limb polarization depends on absorption in a different way than the polarization at large phase angles. It is especially sensitive to a vertical stratification of absorbers. From limb polarization measurements, one can set constraints on the polarization at large phase angles.
Conclusions. The model grid provides a tool for extracting quantitative results from polarimetric measurements of planetary atmospheres, in particular on the scattering properties and stratification of particles in the highest atmosphere layers. Spectropolarimetry of solar system planets offers complementary information to spectroscopy and polarization flux colors can be used for a first characterization of exoplanet atmospheres.
Key words: polarization  scattering  techniques: polarimetric  planetary systems  planets and satellites: general
1 Introduction
Light reflected from planetary atmospheres is generally polarized. The reflection is the result of different types of scattering particles with characteristic polarization properties. Polarimetric observations therefore provide information on the atmospheric structure and on the nature of scattering particles that complements other observations. Systematic model calculations are required to interpret the available polarimetry from solar system planets and prepare for future polarimetric measurements of extrasolar planets.
Scattering processes.
Rayleigh scattering occurs on particles much smaller than the wavelength of the scattered light. This process produces 100% polarization for a single right angle scattering. Rayleigh scattering is much stronger for short wavelengths because the cross section behaves like , and it favors forward and backward scattering, which are both equally strong. The blue sky in Earth's atmosphere is a well known example of Rayleigh scattering by molecules.
Aerosol haze particles with a size roughly comparable to the wavelength can produce strongly forward directed scatterings. Depending on the structure of the particle, a high (p>90%) or low ( %) fractional polarization results for a scattering angle of . For example, the maximum polarization for scattering by optically thin zodiacal or cometary dust is not more than % (e.g. Leinert et al. 1981; LevasseurRegourd et al. 1996), while a polarization close to 100% is inferred for single scattering of haze particles in Saturn's moon Titan (Tomasko et al. 2008).
Liquid droplets in clouds produce a polarization because of refraction and reflection, which can be particularly high (>50%) for scattering angles of about for spherical water droplets, corresponding to the primary rainbow (see e.g. Bailey 2007). Clouds made of ice crystals reflect and refract light in many different ways, and no distinct polarization features like rainbows are expected, except locally, where ice crystals may have very similar structures.
Multiple scatterings in planetary atmospheres randomize the polarization direction of the single scatterings and lower the observable polarization significantly. Therefore the net polarization of the reflected light depends not only on the scattering angle and the properties of the scattering particles, but also on the atmospheric structure. For this reason it is not suprising that a large diversity of polarization properties exists for the solar system planets.
Observations.
Venus shows a low (<5%) negative polarization, which is a polarization parallel to the scattering plane, for most phase angles . In the blue and UV, a rainbow feature with a positive polarization of several percent is present (e.g. Coffeen & Gehrels 1969; Dollfus & Coffeen 1970), indicating that the reflection occurs mainly from droplets in optically thick clouds (Hansen & Hovenier 1974).
For the giant planets, only observations near opposition are possible with earthbound observations. Near opposition the diskintegrated polarization is low because single backscattering is unpolarized and multiple scattering polarization cancels for a symmetric planet.
With diskresolved observations of Jupiter, Lyot (1929) first detected that the Jovian poles show a strong limb polarization of order 510%. To understand this effect one has to consider a backscattering situation at the limb of a sphere, where locally we have a configuration of grazing incidence and grazing emergence (for a plane parallel atmosphere) for the incoming and the backscattered photons, respectively. Photons scattered upwards will mostly escape without a second scattering, and photons scattered down have a low probability of being reflected towards us after the second scattering, but a high probability of being absorbed or undergoing multiple scatterings. Thus photons that are reflected towards us by two scatterings travel predominantely parallel to the surface. Because the polarization angle induced in a single dipoletype scattering process, like Rayleigh scattering, is perpendicular to the propagation direction of the incoming photon, a polarization perpendicular to the limb is produced.
Measurements at large phase angles for Jupiter with spacecrafts detected a polarization of % for the poles while the polarization is much lower (<10%) for the equatorial region (Smith & Tomasko 1984). The high polarization at the poles can be explained by reflection from a scattering aerosol haze layer, while the polarization at the equator is low because of reflection from clouds. Towards short wavelengths (blue) the polarization at the equator increases strongly, indicating that also Rayleigh scattering contributes to the resulting polarization.
For Saturn the polarization is qualitatively similar to Jupiter with an enhanced polarization at the poles at short wavelengths (blue). In the red the polarization level of the poles is lower than for Jupiter (Tomasko & Doose 1984).
Uranus and Neptune display a strong limb polarization along the entire limb (Schmid et al. 2006a; Joos & Schmid 2007). Albedo spectra (e.g. Baines & Bergstralh 1986) and the polarization indicate that Rayleigh scattering is predominant in these atmospheres.
An interesting case is Saturn's moon Titan, which has a thick scattering layer of photochemical haze that produces a very high diskintegrated polarization of % in the B and R band (Tomasko & Smith 1982). More recently the Huygens probe measured the scattering and polarization properties of the aerosol particles in great detail during its descent through Titan's atmosphere (Tomasko et al. 2008).
The observations show that Rayleigh scattering is an important polarigeneric process in atmospheres of solar system objects, in particular for Uranus and Neptune, and for the equatorial regions of Jupiter and Saturn. Besides Rayleigh scattering one has to consider the reflection from haze particles (aerosols). Scattering by small aerosol particles may be approximated by Rayleigh scattering. For large particles, , the strong forward scattering effect and the reduced polarization for right angle scattering cause significant differences when compared to Rayleigh scattering.
Clouds dominate in the atmosphere of Venus, and at longer wavelengths (red) also in Saturn and Jupiter. The reflection from clouds produces only a low positive or even negative polarization signal in Venus, Saturn or Jupiter, typically at a level p <5%. In a first approximation one may therefore treat clouds like a diffusely scattering layer producing no polarization.
Polarimetric measurements of stellar systems with known extrasolar planets were attempted, but up to now no convincing detection of the polarized reflected light from an extrasolar planet has been made (Lucas et al. 2009; Wiktorowicz 2009). The deduced upper limits on the polarization flux from the closein planet indicate that these objects are not covered with a well reflecting Rayleigh scattering layer.
Model calculations.
The classical theory for the analytic solution of the multiple scattering problem is treated in the seminal work of Chandrasekhar (1950), from which the polarization of conservative (nonabsorbing) Rayleigh scattering planets can be derived. Van de Hulst (1980) gives a comprehensive overview on theoretical work up to that time including many numerical model results.
Schmid et al. (2006a) put together available model results useful for parameter studies of the polarization from Rayleigh scattering atmospheres. This includes the following model results:
 phase curves for the diskintegrated intensity and polarization for finite, conservative (no absorption) Rayleigh scattering atmospheres for different optical thicknesses and ground albedos from Kattawar & Adams (1971);
 the limb polarization at opposition for semiinfinite Rayleigh scattering atmospheres with different single scattering albedos derived from formulas and tabulated functions given in Abhyankar & Fymat (1970, 1971) and Chandrasekhar (1950);
 the limb polarization at opposition for finite, conservative (no absorption) Rayleigh scattering atmospheres for different optical thicknesses and ground albedos from tabulations given in Coulson et al. (1960).
Another line of investigation now concentrates on the expected polarization of extrasolar planets. The Rayleigh and Mie scattering polarization of closein planets was investigated by Seager et al. (2000). These calculations consider planets which are unresolved from their central star and the polarization signal is strongly diluted by the unpolarized stellar light.
Stam et al. (2004) modeled the polarization of a Jupiterlike extrasolar planet with methane absorption bands for three special cases and presented polarization spectra and wavelength integrated phase curves. Also monochromatic phase curves for a nonabsorbing clear and a hazy atmosphere are available (Stam et al. 2006). Other studies determined the expected polarization from clouds of terrestrial planets (e.g. Bailey 2007) or the polarization of extrasolar analogs to Earth (Stam 2008).
Despite all these models systematic model calculations are sparse in the literature. For finite Rayleigh scattering atmospheres, polarization phase curves have been calculated only for few selected cases. No results are available for the limb polarization of atmospheres with finite thickness and absorption.
It is the goal of this paper to present a grid of model results for Rayleigh scattering models with absorption and to explore the model parameter space in a systematic way. The results should allow a comparison with observations and provide a tool for their interpretation. Additionally effects of selected deviations from simple Rayleigh scattering models will be discussed.
In the next section the paper describes our scattering model and the Monte Carlo simulations. Section 3 presents the results from a comprehensive Rayleigh scattering model grid covering the three atmosphere parameters: single scattering albedo , optical thickness of the Rayleigh scattering layer , and albedo of the underlying reflecting surface . In Sect. 4 we explore the effects of a mixure of isotropic and Rayleigh scattering, of particles with a forward scattering phase function, and of two polarizing layers. In Sect. 5 we discuss spectral dependences. Section 6 highlights some special cases and diagnostic diagrams which may be of particular interest for the interpretation of observational data. A discussion and conclusions are given in the final section. Appendix A describes the tables with the numerical results of our calculations of intensity and polarization phase curves for a grid of 333 model parameter combinations. These are available in electronic form at the CDS.
2 Model description
Our planet model consists of a spherical body of radius R, illuminated by a parallel beam. This geometry is appropriate for not rapidely rotating planets with a large separation, , from the parent star. Each surface element is approximated by a plane parallel atmosphere. This simplification is reasonable for planets without an extended, tenuous atmosphere.
2.1 Intensity and polarization parameters
The intensity and polarization of the reflected light is described by the
Stokes vector
.
The linear polarized
intensity or polarization flux is defined by the parameters
Q=I_{0}I_{90} and
U=I_{45}I_{135}, where the indices
stand for the polarization direction with respect to a specified direction
in the selected coordinate system. In this paper only processes producing
linear polarization are studied and therefore the Stokes parameter V
for the circular polarization is omitted.
We express the fractional polarization by the symbols
(1) 
and the polarized intensity
(2) 
For the study of the limb polarization in resolved solar system planets at opposition we introduce the radial Stokes parameter Q_{r}, which is positive for an orientation of the polarization parallel to the radius vector (perpendicular to the limb) and negative for an orientation perpendicular to . The Stokes U_{r} parameter is the polarization direction to the radius vector (see e.g. Schmid et al. 2006a, for an illustrative description of the radial polarization). The polarization fraction is represented by q_{r} and u_{r}.
The radial polarization curves q_{r}(r) and Q_{r}(r) can only be observed if the planetary disk is well resolved. The measured radial profile depends strongly on the achieved spatial resolution. Because of the limited spatial resolution of most observations it is very hard to exactly measure the polarization near the limb. It is much less difficult to evaluate a diskintegrated polarization or polarization flux and to estimate and correct the degradation of the observed value with respect to the intrinsic value with a simulation of the observational resolution or point spread function. This approach is described in detail in Schmid et al. (2006a) for seeing limited polarimetry of Uranus and Neptune.
Therefore we mainly discuss the intensity weighted polarization , which is the equivalent to the diskintegrated radial polarization normalized to the geometric albedo. The geometric albedo is the diskintegrated reflected intensity of a given model at opposition normalized to the reflection of a white Lambertian disk. It corresponds to in our calculations.
The radial polarization curves are qualitatively similar for most models. The shape of the intensity curve varies significantly from limb darkening to limb brightening for different model parameteres and cannot solely be described by the geometric albedo. Additionally we choose the Minnaert law exponent k as fit parameter for the shape of the centertolimb intensity curve. The Minnaert law for opposition is , where . This yields the following oneparameter fit curve I(r) = I_{r=0} (1r^{2})^{k1/2}.
2.2 Atmosphere parameters
The plane parallel atmosphere is assumed to consist of a homogeneous scattering layer that is either semiinfinite or finite with a reflecting (cloud or ground) Lambertian surface layer with a surface albedo. The basic model atmospheres are described by three parameters:
 the single scattering albedo ;
 the (vertical) optical thickness for scattering, , of the scattering layer;
 the albedo of the surface below the scattering layer.
(3) 
The value indicates pure scattering (no absorption) while is the other extreme of no scattering and just absorption (e.g. black dust). Similarly, a surface albedo of corresponds to a black surface, while a perfectly white Lambertian surface is defined by .
The optical depth for scattering
follows from the column density Z of the scattering layer:
,
where
is the scattering cross section per particle.
The semiinfinite case corresponds to
.
We treat absorption like an addition of absorption optical depth to a
layer with a given scattering optical depth
,
which is equivalent to reducing the single scattering albedo. This approach is suited for discussing the reflected
intensity and polarization inside and outside of absorption features
like CH_{4} or H_{2}Obands, where
differs dramatically while
is essentially equal.
Then the total optical thickness
of the layer including absorption
is given by
(4) 
The basic model grid (Sect. 3) considers only Rayleigh scattering ( , ) as scattering process and Lambert surfaces with an albedo below the scattering layer. Extensions, such as including nonpolarizing isotropic scattering where , haze layers or more than one scattering layer are discussed in Sect. 4.
2.3 Geometric parameters
The geometric parameters describe the location of the considered surface point P and the escape direction of the photons (Fig. 1). A global coordinate system describes the orientation of the planet with respect to the star. Its polar axis is the surface normal at the substellar point S', and the location of each point P is described by polar angle and azimuthal angle (not drawn). is also the photon's angle of incidence at point P. The escape direction, i.e. the location of the observer, is given by a polar angle and azimuthal angle (not drawn). is equivalent to the phase angle defined by the three (central) points: star or sun S, planet 0, and observer E (Earth).
For the description of the scattering processes, a local coordinate system is set up at point P for the plane parallel atmosphere with surface normal z perpendicular to the planet surface in P, polar angle and azimuthal angle .
Figure 1: Model geometry. The dashed line represents the trajectory of a reflected photon. 

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In general, each point P can have individual atmospheric properties. Then
the model outputs, the Stokes vector components I, Q and U, depend each on seven parameters:
This description allows calculation of the reflected intensity and polarization of each surface point on the illuminated hemisphere viewed from any direction. Obviously this large parameter space needs to be simplified for a first parameter analysis. If we adopt the same atmospheric structure everywhere on the planet, and are no longer functions of and and we obtain a rotationally symmetric model geometry with respect to the line S0, which is independent of the azimuthal angle .
For extrasolar planets it will not be possible to resolve the disk in the near future. For diskintegrated results we can eliminate the dependence of the reflected intensity and polarization on the surface point parameters and . Because of the rotational symmetry of the geometric model, the intensity and the polarization then only depend on the polar viewing angle or phase angle . Moreover the orientation of the polarization signal is either parallel or perpendicular to the scattering plane (the plane S0E), which we call the Qpolarization direction. Q is defined positive for a polarization perpendicular to the plane S0E and negative for a polarization parallel to this plane. The Upolarization is zero in this coordinate system for symmetry reasons.
For the full disk the integrated intensity and polarization signals from a planet
depend on the following parameters:
For solar system planets at opposition we obtain a rotationally symmetric scattering geometry (viewing direction is identical to the axis of symmetry of the geometric model). We then have a scattering model which depends only on or the normalized projected radius , and which is independent of . The resulting polarization will be in the radial direction either parallel or perpendicular to the radius vector and therefore our model output is the radial Stokes parameter Q_{r} (cf. Sect. 2.1). The Stokes U_{r} parameter again has to be zero for a spherically symmetric planet.
For exact opposition the dependences of the scattering model results
can be described by the following parameters:
These are the center to limb intensity curve and the center to limb radial polarization curves which both depend only on the atmospheric parameters.
2.4 Monte Carlo simulations
For our simulations we used the Monte Carlo code described in Schmid (1992), which was slightly adapted for the case of light reflection from a planet. Basically the code calculates the random walk histories of many photons in the planet model atmosphere until the photons have escaped or are destroyed by an absorption process. After a sufficiently large number have escaped, the scattering intensity and polarization of the reflected light can be established for different lines of sight. In our calculations we assume that despite multiple scatterings the escaping photons emerge at the same point where they penetrated into the planet. In each scattering process the photon undergoes a direction and polarization change calculated from the appropriate phase matrix. The linear polarization of the photons in the simulations is defined by the orientation of the electric vector for the photon's electromagnetic wave. In a given coordinate system we can then evaluate the contribution to the Stokes intensity for each photon in and direction.
The escaping photons have to be collected in discret direction bins (in our models phase angles with a finite bin width ) to evaluate and . These are then a mean photon intensity and polarization for that bin. should be small to resolve any structure in and , but also sufficiently large to collect enough photons for results with small statistical errors. The aim of our simulations is to reach at least the expected precision of observational data. The rotational symmetry imposed on our models helps to increase the bin size for the phase curve interval , which behaves like . This means that we have to divide the photon count per bin by the factor . The intensity is obtained by normalizing with the reflectivity of a white Lambertian disk. For a given simulation the relative statistical errors (photon shot noise) are particularly good for , much less favorable for and very bad for where only a few photons will be collected, because the irradiated hemisphere of the planet is almost invisible for this phase angle. For the centertolimb curves we bin uniformly in with a bin size of , which requires an additional normalization by .
The number of photons per model was chosen such that the number of reflected photons in phase angle bins relevant for observations ( ) are about when integrated over the whole disk. This corresponds to an error in polarization %. For the radial curves the total number of photons was increased such that the same precision was reached in most radial bins. No photons emerge at the exact phase angle . Therefore for the limb polarization calculations we count all photons that are in the bin , even though the calculation for the radial polarization includes the assumption that . The error induced by this measure is smaller than the statistical error.
A general guideline for the Monte Carlo technique for random walk problems is given in Cashwell & Everett (1959) and many Monte Carlo simulations for the investigation of light scattering are described in the astronomical literature (see e.g. Witt 1991; Code & Whitney 1995; Wolf et al. 1999). In Schmid (1992) a detailed description on many aspects of the employed Monte Carlo code are given; e.g. the general scheme of the code, the required transformations between the involved coordinate systems (starplanet, planetplane parallel atmosphere, atmospherephoton), the determination of the free path length, the treatment of isotropic scattering and Rayleigh scattering according to the Rayleigh phase matrix, an assessment of statistical errors, and a comparison with analytical calculations.
3 Model results for a homogeneous Rayleigh scattering atmosphere
This section discusses the model grid results for simple homogeneous Rayleigh scattering atmospheres described by parameters , and (cf. Sect. 2.2) We discuss phase curves (Sect. 3.1) and radial profiles (Sect. 3.2) for selected cases and explore the full parameter space for diskintegrated results at and (Sect. 3.3).
Many of the general dependences of these model results on atmospheric parameters were already discussed in previous studies mentioned in the introduction (Sect. 1). Compared to these our calculations are much more comprehensive and the extensive model grid results are provided in electronic form (see Appendix A). An overview of the dependence of observable quantities, such as intensity, fractional polarization and polarized intensity, on atmosphere parameters is presented in diagrams which may be useful for the interpretation of observational data.
The results presented in this section are in very good agreement with the previous calculations in Kattawar & Adams (1971), Stam et al. (2006) and Schmid et al. (2006a).
3.1 Phase curves
Figure 2: Left: phase dependence of the intensity I, fractional polarization q and polarized intensity Q for Rayleigh scattering atmospheres. Right: radial dependence of the intensity I, radial polarization q_{r} and radial polarized intensity Q_{r} at opposition. Line styles denote: semiinfinite case (solid) for single scattering albedos (thick), 0.1 (thin) and finite atmosphere ( ) with (dashed) and 0.6 (dashdot) for surface albedos (thick) and 0 (thin). Also shown is the intensity curve for conservative semiinfinite isotropic scattering (dotted). 

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For the investigation of extrasolar planets, the phase dependence of the diskintegrated polarization is of interest. We discuss the phase curve for selected model cases (Fig. 2, left): a semiinfinite and a finite scattering layer with different absorption properties of the scattering and surface layers.
The semiinfinite, conservatively scattering layer is a good reference case for an illuminated sphere and is often used for scattering atmospheres. All irradiated light is reflected after one or several scatterings and the spherical albedo is equal to 1. An intensity phase curve for isotropic scattering is given in van de Hulst (1980), and Bhatia & Abhyankar (1982) published a polarization curve for Rayleigh scattering in graphical form, but no tabulated values could be found in the literature.
In our Monte Carlo simulation we treat the semiinfinite atmosphere as and , which yields essentially the same results as an infinite layer but avoids infinite scattering of some photons. Our results of this case are tabulated in Table 1.
Table 1: Reflectivity , polarization fraction and polarized intensity phase curves for a very deep () conservative Rayleigh scattering atmosphere above a perfectly reflecting Lambert surface (surface albedo ).
Intensity:
The intensity phase curves have their maximum at , when the whole illuminated hemisphere is visible, and they decrease steadily to zero at , where only the dark side of the planet is seen. The intensity is equivalent to the geometric albedo. It is 0.7975 for the semiinfinite Rayleigh scattering atmosphere (Prather 1974), higher than for the semiinfinite isotropic scattering model ( , van de Hulst 1980) or a white Lambertian sphere ( ), because the Rayleigh scattering phase matrix favors forward and backward scattering. On the other hand the Rayleigh scattering intensity curve is lower for the range .Of course, the reflected intensity decreases with absorption (with lower single scattering albedo ) in the atmosphere and with the albedo of the underlying surface layer. The effect of absorption in the scattering atmosphere is important for thick layers, while the albedo of the underlying surface is important if the optical depths of the scattering region above is small. A quantitative description of these dependences is given in Dlugach & Yanovitskij (1974) and Sromovsky (2005b).
Polarization fraction.
The diskintegrated polarization fraction is always zero for phase angles and because of the imposed rotational symmetry. The polarization maximum is near the rightangle scattering configuration .The polarization for the semiinfinite, conservative Rayleigh scattering layer reaches a maximum of q=32.6% for . For reduced scattering albedo, e.g. due to absorption in a molecular band, increases (see e.g. van de Hulst 1980). This happens because absorption strongly reduces the fraction of multiply scattered photons in the reflected light which have randomized polarization directions. If the absorption is very strong then the reflected light consists essentially only of photons that made one single Rayleigh scattering. The polarization phase curve then approaches the Rayleigh scattering polarization phase function with a polarization close to 100 % at .
For finite scattering atmospheres the polarization fraction qalso depends on the albedo of the surface layer. In the models discussed in this section the polarization is only produced in the Rayleigh scattering layer, while reflection from the surface layer is unpolarized. Therefore the resulting polarization is low for a high surface albedo and high for a low surface albedo (see e.g. Kattawar & Adams 1971; Stam 2008). This reflects the relative contribution of the polarized light from the scattering layer with respect to the unpolarized light reflected from the surface underneath.
The peak of the polarization curve is shifted towards large phase angles ( ) for models with thin scattering layers and high surface albedos, as previously described by Kattawar & Adams (1971). At large phase angles ( ), when only a planet crescent is visible, the fraction of scattered photons hitting the planet initially under grazing incidence is relatively high. For a thin scattering layer grazing incidence helps to enhance the probability for a polarizing Rayleigh scattering. For this reason the polarized light from the Rayleigh scattering atmosphere is less diluted by unpolarized light reflected from the surface at large phase angles and the fractional polarization is higher.
Polarized intensity.
The polarized intensity , which is the product of polarization q and intensity I, is zero at and , while the maximum of the phase curve is near , depending slightly on the model parameters. The maximum value for the polarized intensity, considering the entire parameters space, is for the semiinfinite, conservative Rayleigh scattering atmosphere at . It seems unlikely that another type of scattering process and model atmosphere can produce a higher polarized intensity.The polarized intensity decreases with increasing absorption, because the drop in intensity is stronger than the increase in fractional polarization. The polarization flux is a rough measure for the number of reflected photons undergoing one single Rayleigh scattering. Second and higher order scatterings also add to the polarized intensity, but only at a much lower level. Adding absorption can only reduce the number of such scatterings and therefore diminishes the polarized intensity.
A very important property of the polarization flux Q is that it does not depend on the albedo of the surface layer (assumed to produce no polarization) below the scattering region.
3.2 Radial dependence for resolved planetary disks at opposition
For the interpretation of the limb polarization of solar system objects close to opposition, we discuss the radial or centertolimb dependence of the intensity I(r), the radial polarization q_{r}(r) and the radial polarized intensity Q_{r}(r) (Fig. 2, right) for the same model parameters as for the phase curves in Sect. 3.1.
Intensity:
The radial intensity curve I(r) shows a pronounced limb darkening in the semiinfinite conservative case. For a strongly absorbing atmosphere, e.g. within an absorption band, the I(r)curve becomes essentially flat. Thus for an absorbing (and homogeneous) semiinfinite atmosphere limb brightening cannot be produced. For comparison the centertolimb intensity curve I(r) for isotropic scattering and for a Lambert sphere ( ) are also shown.For finite scattering atmospheres with an optically thin layer the centertolimb intensity curve can show a limb brightening effect. Limb brightening occurs for a highly reflective scattering layer (high ) located above a dark surface (low ), e.g. a thin aerosol layer or a methanepoor layer above the methanerich absorbing layer (e.g. Price 1978). Limb brightening is observed in solar system planets in deep absorption band (e.g. Karkoschka 2001; Sromovsky & Fry 2007). Limb brightening is investigated in more detail in Sect. 3.2.1.
Radial polarization fraction:
The radial polarization fraction q_{r}(r) is always zero in the disk center because of the symmetry of the scattering situation. For all cases the polarization increases steadily towards the limb and reaches a maximum value close to the limb between r=0.95 and 1.0. The polarization q_{r}(r) is always positive, which means a radial polarization direction or limb polarization perpendicular to the limb.It is important to note that the limb polarization decreases with decreasing single scattering albedo (more absorption) in contrast to the situation at large phase angles. This indicates that the photons producing the limb polarization are more strongly reduced by absorption than the reflected ``unpolarized'' photons.
The explanation is that singly scattered (i.e. backscattered) photons do not contribute to the limb polarization, while reflected photons scattered twice or a few times are responsible for the largest part of the limb polarization. Absorption implies that a larger fraction of escaping photons are singlyscattered and therefore unpolarized at opposition. Note however that for the semiinfinite atmosphere, the maximum radial polarization is not reached in the conservative case. A slightly lower scattering albedo ( ) mostly reduces the amount of highest order scatterings and thus the polarization fraction is somewhat enhanced when compared to the conservative case (see Schmid et al. 2006a, and Fig. 7 in Sect. 3.3).
The fractional limb polarization q_{r}(r) for finite scattering layers depends strongly on the albedo of the underlying surface : q_{r}(r) is high for low and low for high like for large phase angles. A low surface albedo decreases the photons with multiple scatterings in the plane perpendicular to the limb, which are polarized parallel to the limb, thus enhancing the polarization in perpendicular direction. Therefore the limb polarization of a bright layer over a dark one can be even higher than for a semiinfinite atmosphere. This is discussed in more detail in Sect. 3.3.
Radial polarized intensity:
The radial polarized intensity increases with r from zero in the disk center to a maximum at r>0.9 and then drops at the very limb. For semiinfinite atmospheres, Q just decreases at all radii with decreasing single scattering albedo .For finite atmospheres, the limb polarization flux Q_{r}(r) depends only slightly on the surface albedo. Decreasing from 1 to 0 can increase Q_{r}(r) at most for some models, while for most models Q_{r}(r) is virtually constant. This is similar to the case for large phase angles.
3.2.1 Limb darkening and limb brightening vs. limb polarization
For a surface with a low albedo below a thin scattering layer the limb can be brighter than the disk center, an effect that is generally called limb brightening. In principle this effect should be called ``a central disk darkening'', because the low surface albedo does not brighten the limb. It only absorbs more light in the center of the disk, where a higher fraction of photons reach the absorbing surface because of their perpendicular incidence when compared to the situation of grazing incidence at the limb. Despite this fact we will retain the term ``limb brightening'' and consider the limb brightness on a relative scale compared to the brightness of the disk center.
The limb darkening and limb brightening effect can be parametrized to a first order using the Minnaert law I(r) = I_{r=0} (1r^{2})^{k1/2}. The Minnaert parameter k determines the shape of the curve, k=1 corresponds to Lambert's law, k=0.5 to a flat intensity distribution I(r) = I_{0} and k < 0.5to limb brightening. The k parameter was determined by fitting Minnaert's law to all modeled intensity profiles, fixing the intensity at the center and excluding the outermost point where the formula diverges for k<0.5. With the exception of some cases mentioned below, most profiles can be fitted adequatly.
In Fig. 3 different examples of limb darkening and limb brightening are shown along with the best fit of the Minnaert law. Intensities are normalized to the central disk intensity. There are two types of limb brightening curves. For very thin atmospheres the maximal brightness is measured at the very edge of the planet, while for a moderate optical depth the intensity raises slightly up to a certain radius (e.g. 0.9 R_{p}) and then drops very close to the limb. This second case cannot be fitted with the oneparameter Minnaert law and is approximated here by a relatively flat curve .
Figure 3: Radial intensity curves for different model parameters normalized to the central disk intensity, showing examples of limb darkening and limb brightening. The solid line is the calculated model and the dotted line the best fit with the Minnaert law. (a), (b) and (c) are for conservatively () scattering layers above black surfaces ( ) with scattering layer thickness (a), 1 (b) and (c). (d) is a thin ( ), highly absorbing scattering layer above a white surface ( ). 

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The limiting case of a conservative semiinfinite atmosphere yields a Minnaert parameter of . For going towards 0, k tends to a flat intenstiy distribution k=0.5. For finite atmospheres there is a strong dependence on the surface albedo . For a strongly absorbing atmosphere over a bright surface ( low, high) absorption is more likely towards the limb (k > 1), for a bright atmosphere over a dark surface the opposite is true (k < 0.5). In the latter case the central disk intensity is very low.
Similar to limb brightening, the limb polarization is also enhanced for a bright scattering layer over a dark surface. However, there are fundamental differences between these two effects. Limb polarization arises only for a polarizing process like Rayleigh scattering, while limb brightening occurs also for nonpolarizing scattering processes like isotropic scattering. Additionally limb brightening is the stronger the thinner the upper bright layer, while limb polarization requires a sufficiently thick scattering layer above the dark surface. Finally, limb polarization can also occur for cases of limb darkening, e.g. the semiinfinite, conservative atmosphere. Therefore, the two effects provide complementary diagnostics of the vertical structure of the atmosphere.
3.3 Parameter study for quadrature phase and opposition
This section explores the full parameter space for simple Rayleigh scattering atmospheres. We explore the parameter space by varying one of the three parameters , and (cf. Sect. 2.2) while fixing the other two. We study the resulting intensity , polarization fraction , and polarized intensity (Figs. 4 to 6).
The shapes of the model phase curves for the intensity , fractional polarization , and polarized intensity look very similar for different model parameters (see Fig. 2). Therefore it is reasonable for a model parameter study to select the results for the phase angle , considering them as representative (qualitatively) for all phase angles. A phase angle is ideal for extrasolar planets because all planets will pass through this configuration twice during an orbit, regardless of inclination.
The same type of parameter study is presented for the limb polarization of planets at opposition ( ). For this we determine diskintegrated (averaged) quantities for the intensity and radial polarization from the model results (Figs. 7 to 9). The integrated intensity is equivalent to the geometric albedo, is the intensity weighted average of the fractional polarization, and the integrated polarized intensity on the same scale as the integrated intensity. These quantities are determined as described in Sect. 2.1.
Figures 4 and 7 show the dependence on the single scattering albedo . For a given scattering optical depth a reduction in is equivalent to an enhancement of the absorption in the scattering layer. Strong differences in occur in planetary atmospheres for molecular absorptions (e.g. due to CH_{4} or H_{2}O) inside and outside the band while is essentially equal.
In Figs. 5 and 8 the Rayleigh scattering optical depths from to 0.01 are plotted. This illustrates quite well the possible spectral dependence from short to long wavelengths (left to right) for a Rayleigh scattering atmosphere. Since the Rayleigh scattering cross sections is proportional to , it is possible that a planet has at 400 nm and at 800 nm.
The effect of the albedo of the surface below the Rayleigh scattering layer is shown in Figs. 6 and 9.
General results from Figs. 4 to 9 are:
 lowering the Rayleigh scattering albedo always results in a lower intensity I, and lower polarized intensity Q or Q_{r};
 lowering the Rayleigh scattering albedo results in a higher polarization q at large phase angles. Contrary to this the fractional limb polarization q_{r} is reduced for lower ;
 lowering the Rayleigh scattering optical depth produces a strong reduction in the polarized intensity Q or Q_{r} in the optically thin case and causes essentially no change in Q or Q_{r} in the optical thick case ;
 lowering the surface albedo lowers the intensity I and enhances the fractional polarization q or q_{r};
 changing the surface albedo does not change the polarized flux Q and hardly Q_{r}.
Another difference is the influence of on the fractional polarization: q drops with for bright nonpolarizing surfaces and increases for dark surfaces. It is more complicated at opposition: the limb polarization is highest if the dark ground eliminates photons that would otherwise scatter twice perpendicular to the limb, but the atmosphere is still thick enough to produce many photons that escape having scattered twice parallel to the limb. The maximum possible limb polarization % is reached for , and .
Figure 4: Intensity, polarization and polarized intensity at quadrature as function of single scattering albedo for optical depths (solid), 0.6 (dashed), 0.1 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

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Figure 5: Intensity, polarization and polarized intensity at quadrature as function of optical depth for single scattering albedos (solid), 0.8 (dashed), 0.4 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

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Figure 6: Intensity, polarization and polarized intensity at quadrature as function of surface albedo for optical depths (solid), 0.6 (dashed), 0.1 (dashdot) and single scattering albedos ( left), 0.8 ( middle), 0.4 ( right). 

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Figure 7: Geometric albedo, diskintegrated radial polarization and polarized intensity at opposition as function of single scattering albedo for optical depths (solid), 0.6 (dashed), 0.1 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

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Figure 8: Geometric albedo, diskintegrated radial polarization and polarized intensity at opposition as function of optical depth for single scattering albedos (solid), 0.8 (dashed), 0.4 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

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Figure 9: Geometric albedo, diskintegrated radial polarization and polarized intensity at opposition as function of surface albedo for optical depths (solid), 1 (dotted), 0.6 (dashed), 0.1 (dashdot) and single scattering albedos ( left), 0.8 ( middle), 0.4 ( right). 

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From the variation of shown in Fig. 5 it can be seen that the polarized intensity saturates above . Therefore cannot probe deep atmospheric layers. For the intensity and fractional polarization, an absorbing ground under a conservatively scattering layer can be noticed even at .
The polarized intensity consists mostly of photons undergoing just one single Rayleigh scattering. Therefore, Q is not changed by processes which happen deep in the atmosphere or by diffuse scattering on the surface. Q is only reduced if the number of single Rayleigh scatterings are reduced, e.g. because there is only a thin Rayleigh scattering layer or photons are efficiently absorbed high in the atmosphere.
We can approximate the polarized intensity Q
by the following parametrization:
where and are fit parameters. Table 2 shows the best fit parameter , while and are listed in Table 1.
Table 2: Best fit parameter for the parametrization of the polarized intensity Q (Eq. (5)).
For optically thick Rayleigh scattering atmospheres the polarized intensity
Q depends only on the single scattering albedo ,
and the parametrization reduces to:
At quadrature this is
(7) 
For the limb polarization flux the dependence on is much steeper because both I and q_{r}drop with decreasing , as can be seen from the bottom panels of Fig. 7. For thick Rayleigh scattering layers, , the dependence of the limb polarization flux is
(8) 
4 Models beyond a Rayleigh scattering layer with a Lambert surface
The three parameter model grid discussed in Sect. 3.3 provides an overview on basic dependences of simple Rayleigh scattering models. In this section we describe a few results for particle scattering properties different from pure Rayleigh scattering, or models with more than one polarizing scattering layer.
4.1 Atmospheres with Rayleigh and isotropic scattering
Pure Rayleigh scattering is a simplification for planetary atmospheres. Already for Rayleigh scattering by molecular hydrogen one needs to account for a weak depolarization effect, because the diatomic molecule is nonspherical. Another depolarization effect for scattered radiation occurs in dense gas because collisions with other particles take place frequently during the scattering process. In addition aerosols and dust particles can also be efficient scatterers in planetary atmospheres and the net scattering phase matrix differs from Rayleigh scattering and should be evaluated, e.g. by using the more general Mie theory.
A simple way for taking such effects into account in a first approximation is to use a linear combination of
the Rayleigh scattering and isotropic scattering phase matrices
(9) 
where and are the relative contributions of the Rayleigh scattering and isotropic scattering to the total scattering cross section . Note that the single scattering albedo and the scattering optical depth now include both the Rayleigh and the isotropic scattering cross section (cf. Sect. 2.2).
Isotropic scattering is nonpolarizing. If the scattering in the atmosphere is composed of both isotropic and Rayleigh scattering, then the fractional polarization and the polarized intensity are reduced by isotropic scattering, while the intensity is comparable (cf. Fig. 2).
Figure 10 shows the fractional polarization at quadrature as a function of for a few representative cases. In the single scattering limit the decrease is linear, the strongest deviation from a linear law is found for the semiinfinite atmosphere because of the large amount of multiple scatterings. A similar behavior is found for other phase angles, as well as for the radial limb polarization at opposition.
Figure 10: Polarization of atmospheres with Rayleigh and isotropic scattering at 90 as a function of isotropic single scattering albedo , normalized to the case of pure Rayleigh scattering or . Plotted models are: semiinfinite atmosphere (thick solid), , (dashed), , (dashdotted), and (thin solid). All models are without absorption, i.e. . 

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4.2 Forwardscattering phase functions
The high polarization of Jupiter's poles and the diskintegrated polarization of Titan (e.g. Tomasko & Smith 1982; Smith & Tomasko 1984) has been explained by the presence of a thick layer of polarizing haze particles. The derived single scattering properties indicate strong forward scattering and Rayleighlike linear polarization with maximal polarization close to 100% at about 90
scattering angle. Particles that satisfy this behavior are thought to be aggregates that are nonspherical and with a projected area smaller than optical wavelengths (e.g. West 1991). We investigate the polarization properties of a planet with such a haze layer. The particle scattering properties are implemented as described in Braak et al. (2002) using a simple parametrized scattering matrix of the form
(10) 
where is the scattering angle and
or is the HenyeyGreenstein phase function with the asymmetry parameter g (see e.g. Van de Hulst 1980). g=0 corresponds to isotropic scattering, g=1 to pure forward scattering, g < 0 to enhanced backscattering. Since haze particles have been shown to be strongly forward scattering, we limit our discussion to the two cases g=0.6 and g=0.9.
Figure 11: Probability density function for Rayleigh scattering (solid), HenyeyGreenstein function with asymmetry parameter g=0.6 (dashed) and g=0.9 (dotted). 

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Figure 11 shows the probability density function for in comparison with Rayleigh scattering. The probability density function for the scattering angle is the phase function weighted by and normalized such that the integral over equals 1. From this function the probability of the scattering angle within a certain interval is calculated by integrating over this interval. One can see that for the haze models small scatttering angles (foward scattering) are greatly enhanced in comparison to Rayleigh scattering, while the probability for backscattering is much lower.
describes the fractional polarization of the scattered radiation as a function of the scattering angle. For scattering on haze particles it can be similar to Rayleigh scattering scaled by a factor p_{m}, the maximal single scattering polarization at scattering angle. For a first qualitative analysis we set p_{m}=1 which is an upper limit that may slightly overestimate the resulting polarization. The other matrix elements are identical to Rayleigh scattering.
Figures 12 and 13 show the phase and radial dependences for the haze models similar to the Rayleigh scattering case in Sects. 3.1 and 3.2.
Intensity:
The phase curves of the haze models differ from the Rayleigh scattering models mainly at small phase angles. The geometric albedo is lower for the haze models because backscattering is strongly suppressed compared to Rayleigh scattering. This is already discussed by Dlugach & Yanovitskij (1974), who calculated albedos for semiinfinite hazy atmospheres. Our calculations result in slightly higher albedos because of the inclusion of polarization. At phase angles around 90 the intensities are very similar for all models for nonabsorbing atmospheres. An absorber greatly reduces the albedo of a planet with enhanced forward scattering, because many photons penetrate deeply into the atmosphere after the first scattering and then have a high probability of being absorbed. The radial intensity curves mainly reflect the lower geometric albedo, while the shape of the curve is similar for all models.Figure 12: Phase dependence of the intensity I, fractional polarization q and polarized intensity Q for a haze layer. Left: semiinfinite case for single scattering albedos (thick), 0.6 (thin) and g = 0.6 (solid), 0.9 (dashed). The dotted line is the Rayleigh scattering case for comparison. Right: Finite atmosphere with for surface albedos (thick), 0 (thin) and line styles as for the left plot. 

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Figure 13: Radial dependence of the intensity I, radial polarization q_{r} and radial polarized intensity Q_{r} at opposition for a haze layer. Left: semiinfinite case for single scattering albedos (thick), 0.6 (thin) and g = 0.6 (solid), 0.9 (dashed). The dotted line is the Rayleigh scattering case for comparison. Right: finite atmosphere with for surface albedos (thick), 0 (thin) and line styles as for the left plot. 

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Polarization fraction:
The angle of maximal polarization is generally larger for the haze models than for Rayleigh scattering. In the semiinfinite conservative case it is for haze as opposed to for Rayleigh scattering. The shift to larger angles is particularly enhanced for a finite haze layer over a bright Lambert surface. However the maximal polarization decreases with increasing g. For strong absorption, both in or below the scattering layer, the polarization phase curve tends toward the single scattering function like in the Rayleigh case. The fractional limb polarization of haze layers can be much higher than for Rayleigh scattering layers, with diskintegrated values reaching % and peak maxima %. This is understandable because the singly scattered (backscattered) photons which are unpolarized are strongly reduced for foward scattering particles.
Polarized intensity:
The polarized intensity is significantly lower for forward scattering phase functions than for Rayleigh scattering in the phase angle range and for the limb polarization effect at opposition. It drops strongly with increasing g or increasing absorption. Like for Rayleigh scattering the polarized intensity is independent of the surface albedo . The phase curves show a shift of the maximum towards larger phase angles when compared to Rayleigh scattering, in particular for models with thin scattering layers.
4.3 Models with two polarizing layers
Up to now we have treated the region below the scattering layer simply as a Lambert surface with an albedo , which produces no polarization. In this section we explore model results for two polarizing layers with different absorption properties, where the lower layer can be a semiinfinite Rayleigh scattering atmosphere as described in Sect. 3.1.
We focus on the question at what depth of the upper scattering layer the polarization properties of the underlying layer are washed out by multiple scattering and are no longer recognizable in the reflected radiation.
Figure 14 compares the fractional polarization for three cases as a function of scattering optical depth of the upper layer, : a nonabsorbing Rayleigh scattering layer above a semiinfinite, low albedo Rayleigh scattering atmosphere, the same scattering layer above a low albedo Lambertian surface, and an isotropic, nonpolarizing scattering layer above the semiinfinite, low albedo Rayleigh scattering atmosphere.
The reflected polarization shows no dependence on the polarization properties of the underlying surface for deep scattering layers with . There are too many multiple scatterings to preserve this type of information from deeper layers in the escaping photons. An imprint from the polarization of the lower layer becomes visible for thin scattering layers with . Particularly well visible is the polarization dependence on for the case where a polarizing layer is located below an isotropically scattering layer. The polarizing lower layer only becomes apparent for .
The same is true for the polarized intensity, because the reflected intensity only shows a very weak dependence on the phase function of the scattering layer. The effects are also very similar for the limb polarization at opposition.
Figure 14: Fractional polarization q as function of of the upper layer at quadrature for models with Rayleigh scattering (solid) or isotropic (dotted) upper layer, and semiinfinite Rayleigh scattering lower layer with (thick) or Lambertian lower layer with A=0.2 (thin), which provides the same reflectivity. 

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5 Wavelength dependence
The wavelength dependence of the reflected intensity and polarization of a model planet can be calculated using wavelength dependent parameters , , and or for single or double layer models respectively. These parameters must be derived from a model with a given column density of scattering particles and mixing ratios for Rayleighscattering and absorbing particles.
As an example we selected parameters which approximate very roughly an Uranuslike atmosphere (e.g. Trafton 1976) considering only Rayleigh scattering by H_{2} and He and absorption by CH_{4}. In our first example we look at a homogeneous scattering layer with methane absorption above a reflecting cloud layer with a wavelength independent surface albedo . This is a strong simplification for Uranus because the methane mixing ratio is of order 100 lower in the stratosphere than in the troposphere (Sromovsky & Fry 2007). Nevertheless it is a useful example for discussing basic effects of the wavelength dependence.
In a second example we make a first approximation for a methane mixing ratio that is varying with height, by having an upper layer of finite thickness without methane and a lower semiinfinite layer that includes methane.
The Rayleigh scattering cross section of molecular hydrogen is given by Dalgarno & Williams (1962)
as
(15) 
where is in Å and in cm^{2}/molecule.
The total Rayleigh scattering optical depth is
(16) 
where Z_{i} is the column density and n_{i} the index of refraction of the ith constituent^{}. We use the same wavelength dependence as for the H_{2} cross section for all constituents. Our upper scattering layer has a column density = 500 kmam.^{} For the atmospheric composition we adopt particle fractions of 0.5% CH_{4} in the single layer case, and a methane free upper layer with 1 % CH_{4} in the lower layer in the two layer case. In all layers the He fraction is 15% and the rest is H_{2}.
Figure 15: Wavelength dependences of the model parameters total optical depth of the upper layer, single scattering albedo or of the upper layer, surface albedo or single scattering albedo of the lower layer. Two cases are considered: a layer of Rayleigh scattering with CH_{4} absorption above a white ( ) Lambert surface (solid), Rayleigh scattering layer without absorption above a deep clear atmosphere with methane absorption (dotted). 

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Because of the strong wavelength dependence of the Rayleigh scattering cross section, changes significantly from the UV to the nearIR (Fig. 15, top panel). Keeping and fixed (no absorber) yields the intensity and polarization results given in Figs. 5 and 8 as function of , which are in this case equivalent to results as function of .
The wavelength dependent single scattering albedo
follows from the CH_{4}
absorption optical depth
and the Rayleigh scattering optical depth according to
(17) 
The absorption cross sections were taken from Karkoschka (1994) and the resulting is shown in Fig. 15.
The intensity , fractional polarization , and polarized intensity is determined from the wavelength dependent model parameters for our two cases at quadrature and opposition (Fig. 16).
Figure 16: Model spectra for the intensity, polarization, and polarized intensity at quadrature ( left) and intensity, radial polarization, and radial polarized intensity at opposition ( right). Lines as in Fig. 15. 

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At quadrature both examples show similar results. In both cases the polarization is enhanced and the polarized intensity is reduced within methane absorption bands, only the changes are less pronounced for a nonabsorbing upper layer. The polarized intensity also drops with wavelength, but it is overall higher in the second case because the polarizing Rayleigh scattering extends to deeper layers. The biggest qualitative difference is seen in the continuum polarization . In the case of an underlying reflecting cloud, drops towards longer wavelengths because of the smaller scattering optical depth above the diffusely scattering cloud. In the second case there is only polarizing Rayleigh scattering and no depolarization effect, so that the increasing absorption with wavelength in the lower layer results in a higher polarization.
Similar spectropolarimetric models but with a Jupiterlike homogeneous atmosphere (higher column density, less methane than in our example) above both a dark surface and a reflecting extended cloud were discussed by Stam et al. (2004) for . The qualitative behavior of intensity and polarization with wavelength is quite similar to our example. However, for the same column density and methane fraction we find a significantly lower intensity and higher polarization within methane bands. The origin of this discrepancy is unclear. A further comparison with intensity calculations for a Neptunelike atmosphere by Sromosvky (2005a) shows a very good agreement at all wavelengths. Based on this we conclude that our model spectra should be correct.
Intensity and polarized intensity at opposition behave qualitatively similar to the large phase angle case. However the fractional polarization is completely different. Absorbing particles in the upper layer tend to reduce the fractional limb polarization, while absorption in the lower layer enhances it. Observations of the limb polarization of Uranus and Neptune (Joos & Schmid 2007) show that the fractional polarization is indeed enhanced within methane bands. Clearly for modeling limb polarization of these planets in absorption bands it is important to take into account the proper vertical stratification of the absorbing component. A detailed model accounting for methane saturation and freezeout to fit the observations is beyond the scope of this paper.
6 Special cases and diagnostic diagrams
We explore some special and extreme model cases in diagnostic diagrams of observational parameters for phase angle and opposition.
6.1 Fractional polarization versus intensity
Figure 17 displays the diagnostic diagram for the reflectivity and the relative polarization at phase angle . Also indicated are the isocontours for the polarization flux .
The diagram shows points for special model cases and curves for the dependence on specific model parameters. The shaded area defines the area of observational parameters covered by our 3parameter model grid for Rayleigh scattering (Sect. 3). Including isotropic scattering (Sect. 4.1) or having a vertically inhomogeneous atmosphere (Sect. 4.3) does not expand the covered area.
Figure 17: Intensity vs. polarization at quadrature for the grid models. The shaded area indicates the possible range for Rayleigh and isotropic models. The symbols and lines indicate: semiinfinite conservative Rayleigh scattering (square), Lambert sphere (round), and black planet (diamond). The dashdotted line shows semiinfinite models, the dashed and full line finite models without absorption () with surface albedo and 0 respectively. The haze models shown in Fig. 12 are indicated by crosses (high albedo) and plusses (low albedo). 

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Figure 17 emphasizes that it is not possible to have a Rayleigh scattering planet with both very high albedo and polarization. A high albedo implies either a lot of multiple or isotropic scattering, which both reduce the fractional polarization. On the other hand a high polarization implies mainly single scattering and therefore strong absorption and a low reflectivity. The maximal polarization at a fixed intensity is given by the model with a conservative scattering layer over a dark ( ) surface and appropriate . The semiinfinite atmosphere with varying gives only slightly lower results than the former models. The maximum of the product is reached for the conservative semiinfinite atmosphere ( ). Since the polarized intensity Q is independent of the surface albedo , a change in is equivalent to a shift along the Q isocontours in the diagram.
Figure 18: Geometric albedo vs. diskintegrated radial polarization at opposition for the grid models. The models are the same as in Fig. 17. 

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The diagram also indicates the location of the haze models discussed in Sect. 4.2. Most of the haze models lie within the same area as Rayleigh scattering. Only for very thick haze layers with high singlescattering albedo is it theoretically possible to get somewhat higher fractional polarization for a given intensity.
Figure 18 is the same diagram at opposition for the geometric albedo , the diskintegrated limb polarization and isocontours for the radial polarized intensity . Like for large phase angles, the limb polarization for fixed intensity is highest for the conservative Rayleigh scattering layers over a dark surface. However, for the polarization drops to 0%, while at large phase angles with it raises towards 100% when the few reflected photons are mainly singly scattered. The semiinfinite models provide a distinctly lower fractional polarization signal than a finite conservatively scattering atmosphere over a dark surface. The fractional limb polarization for very low albedos can be significantly higher for atmospheres with haze than for Rayleigh scattering, because the unpolarized backscattering is greatly reduced.
For models with two polarizing layers with different absorption properties, the results are located in the same area as for one layer above a surface. The limiting cases are models with a completely dark lower layer (equivalent to a dark surface), and two identical layers (equivalent to a single semiinfinite layer). For atmospheres that contain also isotropically scattering particles the polarization is always lower and the intensity either slightly enhanced or reduced depending on because of the different scattering phase functions.
Figure 19: Diskintegrated radial polarization at opposition vs. polarization at quadrature for the grid. The models are the same as in Fig. 17. All Rayleigh scattering models lie in the dark shaded area, (partly) isotropic models also in the light shaded area. 

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6.2 Polarization near versus limb polarization
For the prediction or the future interpretation of the polarization of extrasolar planets it is of interest to compare the polarization at phase angles near quadrature with the limb polarization at opposition.
Figure 19 shows a diagram for the fractional polarization and the fractional limb polarization . Again the special models are indicated with black symbols and lines as in Figs. 17 and 18.
A lower limit for the polarization fraction at phase angles can be set from the limb polarization at opposition for Rayleigh scattering or partly isotropic scattering atmospheres. For example a limb polarization of % implies a minimal polarization of %. The upper limit for the polarization fraction ) is not well constrained by . The lower limit for Rayleigh or isotropic scattering may overestimate the polarization at large phase angles only for very thick and bright haze layers.
A tighter correlation is obtained for the polarization flux and the limb polarization flux , which is shown in Fig. 20. All Rayleigh scattering models are located in a narrow area along a line from the origin (Lambert sphere / black planet) to the semiinfinite, conservative Rayleigh scattering model. Thus, for Rayleigh scattering atmospheres, one can predict the large phase angle polarization flux from the limb polarization flux and vice versa. The area is slightly broadened if isotropic scattering is included in the models, but the relation still holds quite well. Only very thick and high albedo haze layers show a significantly lower ) for a given .
6.3 Broadband polarized intensity
Color indices of observational parameters are often relatively easy to measure and they are helpful for the characterization of atmospheres. From the atmosphere models they are obtained by averaging spectral results (Sect. 5) over the filter bandwidths.
Figure 20: Diskintegrated radial polarized flux at opposition vs. polarized flux at quadrature for the grid models. The indicated models are the same as in Fig. 17. All Rayleigh scattering models lie in the dark shaded area, (partly) isotropic models also in the light shaded area. 

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Here we discuss the colors for a Rayleigh scattering atmosphere with methane as a main absorber. It is investigated how the polarized intensity color changes as a function of methane mixing ratio and column density above a cloud or surface. Color indices are calculated by integrating over the wavelength range foreseen for filters in the SPHERE/ZIMPOL instrument (Beuzit et al. 2006). The filters are assumed to have flat transmission curves with cut offs at 555 and 700 nm (Rband) and 715 and 865 nm (Iband). We concentrate on the color index of the polarized intensity Q_{I}/Q_{R} (Fig. 21).
The polarized intensity is higher at shorter wavelengths, and Q_{I}/Q_{R} < 1 for all models because of the decrease of the Rayleigh scattering cross section with wavelength and the general increase of the absorption cross section of methane with wavelength. Q_{I}/Q_{R} is near 1 only for very thick atmospheres with very little methane or very thin atmospheres above a surface with wavelength independent scattering properties. In the former case Q_{R} and Q_{I} are very high, in the latter very low. For intermediately thick atmospheres the color index Q_{I}/Q_{R} mainly depends on the methane mixing ratio, while Q_{R} mainly depends on the column density.
From this diagram we may predict that a color index of could be typical for Rayleigh scattering atmospheres with methane absorption. Aerosol particles and absorbers other than methane are expected to have a different spectral dependence of the scattering and absorption cross sections.
Figure 21: Polarized intensity Q_{R} as a function of color Q_{I}/Q_{R} where Q_{R} is the broadband R signal (555 to 700 nm) and Q_{I} the broadband I signal (715 to 865 nm) for Rayleigh scattering planets with methane at 90 phase angle. Indicated are models with constant methane mixing ratios f (dashed) or constant atmosphere column density Z in kmam (dotted) above a Lambert surface. 

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7 Conclusions
This paper presents a grid of model results for the intensity and polarization of Rayleigh scattering planetary atmospheres, covering the model parameter space in a systematic way. The model parameters considered are the single scattering albedo , which describes absorption, the scattering optical depth of the layer , and the albedo of a Lambert surface . The results of these model calculations are available in electronic form at CDS (see Appendix A). In addition we explore models which combine Rayleigh and isotropic scattering, as well as particles with strong forward scattering and atmospheres with vertical stratification.
Simple Rayleigh scattering models are a good first approximation to the polarization of light reflected from planetary atmospheres because some amount of Rayleighlike scattering by molecules or very small aerosol particles can be expected in any atmosphere. From the model grid, which basically provides monochromatic results, the spectropolarimetric signal can be calculated. This is done by considering the wavelength dependence of Rayleigh scattering and absorption in an atmosphere with given column density and particle abundance (see Sect. 5).
The phase curves for the reflected intensity and polarization show a strong dependence on phase but they always have similar shapes (see Fig. 2). However, the absolute level of the phase curve is a strong function of atmospheric parameters such as the abundance of absorbers or aerosol particles, the optical thickness of the Rayleigh scattering layer, or the albedo of the surface layer underneath (Sect. 3 and 4, see also Kattwar & Adams 1971).
The model calculations demonstrate that polarimetric observations would provide strong constraints on the atmospheric properties of the planetary atmospheres. An example is the polarization flux of the reflected light which for optically thick atmospheres is a simple function of the single scattering albedo roughly according to . If both polarization and intensity can be measured, then one can distinguish between highly reflective and absorbing planets with or without substantial layers of Rayleighlike scattering particles.
According to the models a similar diagnostic is possible with observations of the geometric albedo, centertolimb polarization profile, and limb polarization for solar system planets near opposition. The limb polarization is in addition particularly sensitive to the vertical stratification of scattering or absorbing particles located high in the atmosphere.
Table A.1: Extract of model grid results.
The diagnostic potential is further enhanced if data for different spectral features, e.g. inside and outside of absorption bands, or from different spectral wavelength regions can be combined (Sect. 5, see also Stam et al. 2004).
The calculations presented in this work are based on simple atmosphere models and they are therefore mainly useful for a first interpretation of data. For spectropolarimetric data of high quality, which are already available for solar system planets, one should use more sophisticated atmospheric models including a more detailed geometric structure, accurate abundances, and better scattering models for aerosol particles. With such models it might be possible for polarimetric studies to make a contribution to our knowledge on the rather well known atmospheres of solar system objects.
Nonetheless the simple limb polarization models are of interest because they link the model results for large phase angles, suitable for extrasolar planet research, to models which can be easily compared with observations of solar system objects. Thus it may be possible to associate polarimetric observations of extrasolar planets to solar system objects. On the other hand it is possible to predict the expected polarization for quadrature phase of Uranus and Neptunelike extrasolar planets with this simple model grid based on the existing limb polarization measurements of Uranus and Neptune (Fig. 20).
Polarimetric measurements for extrasolar planets are expected in the
near future from high precision polarimeters. The measurements will first
provide the polarimetric contrast, which is the ratio of
the polarization flux from the planet
to the flux of the central star
according to
(18) 
where R is the radius of the planet and D the distance from its central star.
Very sensitive polarimetric measurements of stars with known closein planets already exist, taken e.g. with the PLANETPOL instrument (Hough et al. 2006; Lucas et al. 2009). This instrument measures the polarized intensity of the planet diluted by the unpolarized flux of the central star. It is then difficult to separate the fractional polarization q and the reflected intensity I. D is known from the radial velocity curve, but already the radius of the planet R may be hard to derive if the system shows no transits. For photometrically very stable stars the reflected intensity may be measurable with photometry of the phase curve with high precision instruments like MOST (e.g. Rowe et al. 2008). An uncertainty in the planet radius will affect the precision of the estimation of the normalized reflected intensity (or reflectivity) of the planet.
SPHERE, the future ``VLT planet finder'', which includes the high precision imaging polarimeter ZIMPOL, could provide successful polarimetric detections (Beuzit et al. 2006; Schmid et al. 2006b). This instrument will be able to spatially resolve nearby (d < 10 pc) starplanet systems and allow a polarimetric search for faint companions to stars. In a first step only the differential polarization signal, i.e. the polarization flux , can be measured in the residual halo of the central star. The measurement of the intensity signal might be possible if further progress in techniques like angular differential imaging is achieved. Even if a determination of is possible, an uncertainty remains in the translation to normalized intensity if the radius of the planet is not known.
Thus it may initially be quite difficult to measure intensity and radius. For this reason it is important to investigate the diagnostic potential of the wavelength dependence in the polarization flux in more detail. For example the Rband and Iband yield a polarization color index Q_{I}/Q_{R} from which it should be possible to infer constraints on the Rayleigh scattering optical depth or the strength of absorption bands (see Sect. 6.3). Another route of investigation for atmospheres of extrasolar planets are measurements of the phase dependence of the polarization flux. For example the location of the maximum of Q along the phase curve is sensitive to the presence of aerosol particles, as discussed in Sect. 4.2. For planets in eccentric orbits the dependence of the polarization flux on the separation from the host star can be determined.
One can hope that the current rapid progress in extrasolar planet observations continues, so that intensity measurements and accurate radius estimates for extrasolar planets become available soon after the first polarization flux detections, using the next generation of ground based telescopes and space instruments. Such instruments, if equipped with a polarimetric observing mode, would allow a broad range of observational programs on the reflected intensity and polarization from planets.
Acknowledgements
This work is supported by the Swiss National Science Foundation (SNSF). We thank Harry Nussbaumer and Franco Joos for carefully reading the manuscript.
Appendix A: Model grid tables
Our extensive model grid of intensity and polarization phase curves for homogeneous Rayleigh scattering atmospheres (Sect. 3) is available in electronic form at CDS. Table A.1 shows a sample of the first few lines and columns. The table is structured as follows: Model parameters: Column 1: scattering optical thickness , Column 2: single scattering albedo , Column 3: surface albedo , Model results: Column 4: spherical albedo , Column 5: geometric albedo , Column 6: limb polarization flux , Column 7: , Column 8: ,..., Column 40: Column 41: ,..., Column 74: . Columns 7 to 74 are and spaced in 5 degree intervals. is equivalent to in our calculations. , and are very close to zero for all models and are not listed.
All results are diskintegrated. Binning, normalization and errors are described in Sect. 2.4. For all calculations the number of photons was chosen such that % for phase angles , and therefore %.
The model grid spans the following parameters: , 10, 5, 2, 1, 0.8, 0.6, 0.4, 0.3, 0.2, 0.1, 0.05, 0.01, , 0.99, 0.95, 0.9, 0.8, 0.6, 0.4, 0.2, 0.1, , 0.3, 0. Models for only three values of are given because the polarized intensity is independent of and the intensity drops nearly linearly with increasing . Models with were calculated only for since the results are independent of . Instead of a model with and , we calculated the model with to reduce computation time, but the results are equivalent.
The spherical albedo in Col. 4 is the ratio of reflected photons in any direction to total incoming photons, while the geometric albedo in column 5 is the diskintegrated reflected intensity at opposition normalized to the reflection of a white Lambertian disk. For our sample of Rayleigh scattering models, typically .
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Footnotes
 ... atmospheres^{}
 Full Table A.1 is only available in electronic form at the CDS via anonymous ftp to cdsarc.ustrasbg.fr (130.79.128.5) or via http://cdsweb.ustrasbg.fr/cgibin/qcat?J/A+A/504/259
 ... constituent^{}
 , , .
 ... kmam.^{}
 1 kmam = molecules cm^{2}.
All Tables
Table 1: Reflectivity , polarization fraction and polarized intensity phase curves for a very deep () conservative Rayleigh scattering atmosphere above a perfectly reflecting Lambert surface (surface albedo ).
Table 2: Best fit parameter for the parametrization of the polarized intensity Q (Eq. (5)).
Table A.1: Extract of model grid results.
All Figures
Figure 1: Model geometry. The dashed line represents the trajectory of a reflected photon. 

Open with DEXTER  
In the text 
Figure 2: Left: phase dependence of the intensity I, fractional polarization q and polarized intensity Q for Rayleigh scattering atmospheres. Right: radial dependence of the intensity I, radial polarization q_{r} and radial polarized intensity Q_{r} at opposition. Line styles denote: semiinfinite case (solid) for single scattering albedos (thick), 0.1 (thin) and finite atmosphere ( ) with (dashed) and 0.6 (dashdot) for surface albedos (thick) and 0 (thin). Also shown is the intensity curve for conservative semiinfinite isotropic scattering (dotted). 

Open with DEXTER  
In the text 
Figure 3: Radial intensity curves for different model parameters normalized to the central disk intensity, showing examples of limb darkening and limb brightening. The solid line is the calculated model and the dotted line the best fit with the Minnaert law. (a), (b) and (c) are for conservatively () scattering layers above black surfaces ( ) with scattering layer thickness (a), 1 (b) and (c). (d) is a thin ( ), highly absorbing scattering layer above a white surface ( ). 

Open with DEXTER  
In the text 
Figure 4: Intensity, polarization and polarized intensity at quadrature as function of single scattering albedo for optical depths (solid), 0.6 (dashed), 0.1 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

Open with DEXTER  
In the text 
Figure 5: Intensity, polarization and polarized intensity at quadrature as function of optical depth for single scattering albedos (solid), 0.8 (dashed), 0.4 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

Open with DEXTER  
In the text 
Figure 6: Intensity, polarization and polarized intensity at quadrature as function of surface albedo for optical depths (solid), 0.6 (dashed), 0.1 (dashdot) and single scattering albedos ( left), 0.8 ( middle), 0.4 ( right). 

Open with DEXTER  
In the text 
Figure 7: Geometric albedo, diskintegrated radial polarization and polarized intensity at opposition as function of single scattering albedo for optical depths (solid), 0.6 (dashed), 0.1 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

Open with DEXTER  
In the text 
Figure 8: Geometric albedo, diskintegrated radial polarization and polarized intensity at opposition as function of optical depth for single scattering albedos (solid), 0.8 (dashed), 0.4 (dashdot) and surface albedos ( left), 0.3 ( middle), 0 ( right). 

Open with DEXTER  
In the text 
Figure 9: Geometric albedo, diskintegrated radial polarization and polarized intensity at opposition as function of surface albedo for optical depths (solid), 1 (dotted), 0.6 (dashed), 0.1 (dashdot) and single scattering albedos ( left), 0.8 ( middle), 0.4 ( right). 

Open with DEXTER  
In the text 
Figure 10: Polarization of atmospheres with Rayleigh and isotropic scattering at 90 as a function of isotropic single scattering albedo , normalized to the case of pure Rayleigh scattering or . Plotted models are: semiinfinite atmosphere (thick solid), , (dashed), , (dashdotted), and (thin solid). All models are without absorption, i.e. . 

Open with DEXTER  
In the text 
Figure 11: Probability density function for Rayleigh scattering (solid), HenyeyGreenstein function with asymmetry parameter g=0.6 (dashed) and g=0.9 (dotted). 

Open with DEXTER  
In the text 
Figure 12: Phase dependence of the intensity I, fractional polarization q and polarized intensity Q for a haze layer. Left: semiinfinite case for single scattering albedos (thick), 0.6 (thin) and g = 0.6 (solid), 0.9 (dashed). The dotted line is the Rayleigh scattering case for comparison. Right: Finite atmosphere with for surface albedos (thick), 0 (thin) and line styles as for the left plot. 

Open with DEXTER  
In the text 
Figure 13: Radial dependence of the intensity I, radial polarization q_{r} and radial polarized intensity Q_{r} at opposition for a haze layer. Left: semiinfinite case for single scattering albedos (thick), 0.6 (thin) and g = 0.6 (solid), 0.9 (dashed). The dotted line is the Rayleigh scattering case for comparison. Right: finite atmosphere with for surface albedos (thick), 0 (thin) and line styles as for the left plot. 

Open with DEXTER  
In the text 
Figure 14: Fractional polarization q as function of of the upper layer at quadrature for models with Rayleigh scattering (solid) or isotropic (dotted) upper layer, and semiinfinite Rayleigh scattering lower layer with (thick) or Lambertian lower layer with A=0.2 (thin), which provides the same reflectivity. 

Open with DEXTER  
In the text 
Figure 15: Wavelength dependences of the model parameters total optical depth of the upper layer, single scattering albedo or of the upper layer, surface albedo or single scattering albedo of the lower layer. Two cases are considered: a layer of Rayleigh scattering with CH_{4} absorption above a white ( ) Lambert surface (solid), Rayleigh scattering layer without absorption above a deep clear atmosphere with methane absorption (dotted). 

Open with DEXTER  
In the text 
Figure 16: Model spectra for the intensity, polarization, and polarized intensity at quadrature ( left) and intensity, radial polarization, and radial polarized intensity at opposition ( right). Lines as in Fig. 15. 

Open with DEXTER  
In the text 
Figure 17: Intensity vs. polarization at quadrature for the grid models. The shaded area indicates the possible range for Rayleigh and isotropic models. The symbols and lines indicate: semiinfinite conservative Rayleigh scattering (square), Lambert sphere (round), and black planet (diamond). The dashdotted line shows semiinfinite models, the dashed and full line finite models without absorption () with surface albedo and 0 respectively. The haze models shown in Fig. 12 are indicated by crosses (high albedo) and plusses (low albedo). 

Open with DEXTER  
In the text 
Figure 18: Geometric albedo vs. diskintegrated radial polarization at opposition for the grid models. The models are the same as in Fig. 17. 

Open with DEXTER  
In the text 
Figure 19: Diskintegrated radial polarization at opposition vs. polarization at quadrature for the grid. The models are the same as in Fig. 17. All Rayleigh scattering models lie in the dark shaded area, (partly) isotropic models also in the light shaded area. 

Open with DEXTER  
In the text 
Figure 20: Diskintegrated radial polarized flux at opposition vs. polarized flux at quadrature for the grid models. The indicated models are the same as in Fig. 17. All Rayleigh scattering models lie in the dark shaded area, (partly) isotropic models also in the light shaded area. 

Open with DEXTER  
In the text 
Figure 21: Polarized intensity Q_{R} as a function of color Q_{I}/Q_{R} where Q_{R} is the broadband R signal (555 to 700 nm) and Q_{I} the broadband I signal (715 to 865 nm) for Rayleigh scattering planets with methane at 90 phase angle. Indicated are models with constant methane mixing ratios f (dashed) or constant atmosphere column density Z in kmam (dotted) above a Lambert surface. 

Open with DEXTER  
In the text 
Copyright ESO 2009