We present spatially-resolved, low-resolution (λ/Δλ ∼ 1,500) spectroscopy of the leading hemisphere of Titan in the H-band (1.5–1.7 μm) using adaptive optics. Spatial variations of surface albedo are observed in images at 1.55–1.57 μm, which are clearly distinct from stratospheric haze. There is a significant increase in albedo around the southern (summer) pole at 1.62 μm. Using a plane-parallel radiative transfer model to fit the observed spectra, we find a 61% increase in tropopause haze opacity (τ = 0.100 from 30–40 km) around the southern pole relative to the rest of the disk (where τ = 0.062 from 30–40 km).
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 The dense nitrogen-dominated atmosphere of Saturn's largest moon, Titan, has long intrigued researchers – in part because of the striking similarities to Earth's atmosphere. However, significant differences include both the lack of oxygen and the presence of CH4 [Kuiper, 1944] as the dominant trace species, which together allow for the photochemical production of hydrocarbon aerosols. These aerosols form hazes that globally obscure the surface of Titan at visible wavelengths. In the infrared, where particle opacity becomes sufficiently low, the lower atmosphere and the surface of Titan can be observed.
 Spectroscopic studies complement imaging and have long been useful in determining globally averaged vertical profiles for the various gas-phase hydrocarbons, which are the precursors to atmospheric particulates [Hunten et al., 1984]. It is believed that these particulates are produced photochemically high in the stratosphere (for a review, see, e.g., McKay et al. ), and the hazes they form have been observed to undergo seasonal changes [Lorenz et al., 2001] – likely due to atmospheric circulation [Rannou et al., 2002]. The particulates then settle through the stratosphere and could perhaps serve as condensation nuclei for the clouds that are regularly seen in disk-integrated spectra [Griffith et al., 1998, 2000].
 High-spatial-resolution (AO) imaging alone [Roe et al., 2002b] as well as in concert with 2 μm spectroscopy [Brown et al., 2002] have led to unambiguous detections of clouds near Titan's south pole, highlighting the utility of using these two techniques in tandem. In order to investigate the properties of atmospheric particulates, we present here the first analysis of spatially-resolved 1.6 μm spectra of Titan.
2. Observations and Data Reduction
 Long slit (3.96″ × 0.076″) spectra were recorded with the NIRSPEC/AO system on three nights, 19, 20, and 22 February 2001 UT, at W.M. Keck Observatory, at a spectral resolution λ/Δλ ∼ 1,500. Details of the adaptive optics system may be found in, e.g., Wizinowich et al. . Standard procedures were used to flat field, bias and dark correct the NIRSPEC spectra. Narrowband (H1581) SCAM images of Titan were flux calibrated for normalization of the spectral image maps.
 While the axis along the length of the slit provides a 1-dimensional (latitudinal) spatial axis along a section of Titan's disk, the spectrometer slit must be stepped across the disk (longitudinally) to provide two spatial dimensions for the images of the disk. The full width half-maximum (FWHM) of the observed point spread function (PSF) in images was ∼0.050″. In the reconstructed images the spatial resolution along the slit is ∼0.050″ and perpendicular to the slit the resolution is dominated by the slit width (0.072″) resulting in a spatial resolution of ∼0.090″. Multiple SCAM images (∼5) were recorded, at each slit position, during the spectrometer exposure. The central slit position is determined by calculating the 1-dimensional first derivative of the intensity perpendicular to the long axis of the slit, and then finding the extrema, which identify the edges of the slit positioned on the disk.
 After stepping across the disk with the length of the slit oriented North-South (N-S), one spectrum was recorded at a slit position perpendicular to the previous 10 (E-W). This spectrum is used to scale each of the 10 N-S spectra such that the signal in the regions of spatial overlap between the N-S and E-W spectra match. The spectrum taken E-W along the disk is scaled to the corresponding region of the flux calibrated, narrowband (H1581 filter) SCAM images, with uncertainties in the photometry ∼15%.
3. Results and Discussion
Figure 1 shows a subset of ultra-narrowband images reconstructed from the spectra that are characteristic of the dataset. The first row of images are from 1.55–1.57 μm, where CH4 absorption is weak, and primarily intensity from the surface is measured. The dominant surface feature is the bright feature located at ∼100°W.
 The middle row of images in Figure 1 show that as CH4 opacity increases with wavelength, flux from higher altitude in the atmosphere is observed. At 1.6028 μm the surface dominates the signal, whereas at 1.6158 μm flux from a tropopause haze is observed (see below). At wavelengths longer than 1.6158 μm the bright surface feature is no longer visible. CH4 absorption at this wavelength is strong enough to completely attenuate the light from the sun before it reaches the surface. The observed signal is therefore from photons that are scattered from particulates in the atmosphere.
 The 1.6158 μm image shows that there is a localized enhancement of lower-atmospheric particulates near the southern (summer) pole. This enhancement occurs at the latitude where tropopause cirrus has been detected spectroscopically at 2.1 μm [Griffith et al., 1998; Brown et al., 2002] and has been directly imaged with a narrowband filter at 2.108 μm [Roe et al., 2002b] We show by modelling the observed spectra from this region that this haze is found at 30–50 km, near the tropopause at 42 km.
 At wavelengths longer than 1.6218 μm (bottom row of Figure 1), stratospheric particulates are measured. At these wavelengths the observed flux is diminished, signal-to-noise decreases, and limb brightening becomes more pronounced. The N-S stratospheric haze asymmetry imaged on the same night with an H1702 narrowband filter [Roe et al., 2002a] is seen in the 1.702 μm image and quantitatively modeled below. However, with the narrow bandpass and incomplete spatial coverage of these images we do not clearly observe the E-W asymmetry or polar collar seen by Roe et al. [2002a].
 The pathlength through Titan's atmosphere plays a critical role in determining the observed spectra. Therefore, we first compare spectra measured at the same Titan airmass – that is, points that are equidistant from the center of the disk. Figure 2a shows 8 spectra taken at a Titan airmass of A = 1.12 (0.5 Titan radii, RT, from disk center). The pixel-to-pixel noise of each spectrum is read-noise limited (∼30 DN, or in this case 0.003 I/F) and the similarity of the spectra longward of 1.63 μm is a reassuring consistency check of the data reduction, normalization, image reconstruction and centering.
 Shortward of 1.60 μm the spectra diverge as they probe deeper into the troposphere. The greatest contrast in the spectra occurs at 1.592 μm, where the measurement is sensitive to surface albedo. Figure 2a shows that bright surface features show up in the spectra at 1.592 μm, and that they do not affect the spectra significantly at wavelengths longer than 1.610 μm. This qualitatively indicates that the spectra from 1.61 to 1.64 μm probe an altitude region from the troposphere to the lower stratosphere, and exclude the surface.
 The bright feature seen around the southern pole at 1.62 μm can be investigated by comparing spectra taken from around the limb (A = 2.35, RT = 0.9) of Titan (Figure 2b). A striking feature in these spectra is the increasing divergence at wavelengths shorter than 1.63 μm. The five spectra from the northern hemisphere overlap at 1.61 μm, and contrast with the three spectra from the southern hemisphere at this wavelength. This indicates a robust observational difference between the two sets of spectra.
 A 2-stream approximation solves the radiative transfer equation for plane-parallel layers [McKay et al., 1989]. Line-by-line techniques are used to calculate the absorption coefficients from the methane line parameters compiled in the GEISA database [Husson et al., 1991]. Particles are assumed to scatter as spherical particles, and the Voyager thermal profile is adopted [Lellouch et al., 1989]. The modelled spectra cut off at 1.617 μm as limited by laboratory data for the CH4 spectrum's pressure and temperature dependence. This limitation sets the depth into the troposphere that is accurately modelled to 30 km. Improved laboratory data for weak CH4 transitions in this region would allow analysis of the existing data to probe deeper into the troposphere. Currently, the rich 1.6 μm spectra corresponding to regions below 30 km, where the intriguing cloud and tropospheric haze formation occur, can only be interpreted qualitatively.
 The initial estimate of the haze extinction vertical profile follows a scale height of 21 km. A rudimentary χ2 minimization technique is used to systematically vary the relevant atmospheric parameters – the haze densities in the 9 uppermost layers, the surface albedo, and the CH4 mixing ratio – while determining the mean deviation between the observed spectrum and model output. We fit a series of values (∼10) for each parameter while holding all others at their initial value. The parameter adjustment that yields the smallest χ2 is then updated, and the processes is repeated until the mean squared deviation between the model and the data is below the observation uncertainty (∼20–30 iterations).
 Since multiple solutions for the haze extinction profile give similar values for the minimum χ2 – the extinction may be shown to be anti-correlated in neighboring layers of the model – we select for those extinction profiles that follow the atmospheric scale height with our initial estimate. Profiles that deviate significantly from an exponential decrease with altitude are rejected as unphysical. Changes of a few percent from the best fit optical depths produce modelled spectra outside of the pixel-to-pixel noise of the observations, so uncertainty in the optical depth is estimated to be ∼20%, primarily from the uncertainty in the photometry.
 The extinction profiles of the haze that fit the spectra in Figure 2c are shown in Table 1. The optical depth in the southern polar region from 30–40 km (τS = 0.100) is almost double the corresponding region from the northern hemisphere (τN = 0.062). At higher altitude in the stratosphere (90–150 km) the haze optical depth is greater in the North than in the South, which is in agreement with narrowband images at 1.702 μm [Roe et al., 2002a]. The total haze optical depths in both the North and South agree with values derived from 2 μm images [Gibbard et al., 2004].
Table 1. Comparison of Altitude Dependence of Stratospheric Haze Layers in the Northern Mid Latitudes and Near the Southern Pole.
 The best fit profiles follow the atmospheric number density scale height [Yelle et al., 1997], h = 18 km from 0–60 km and h = 35 km from 80–200 km. This is in general consistent with current microphysical models of particle settling [McKay et al., 2001; Luz et al., 2003] and consistent with extinction profiles determined from modelling 0.89–0.95 μm narrowband HST images [Young et al., 2002].
 Sensitivity tests for the altitude of the lower-stratospheric haze layers, in particular the altitude of the enhancement in the southern hemisphere, are shown in Figure 2d. Systematically shifting the haze opacity parameters down by one layer clearly under-predicts the signal at 1.62 μm and the slope of the spectrum as it increases toward shorter wavelengths. Exchanging the values for haze opacity at 30 and 40 km – representing a haze enhancement higher in the atmosphere – is a much more subtle effect, but nonetheless produces a spectrum that is outside of the observational error. This indicates that while the observed haze may extend slightly below the tropopause, is does not extend deep into the troposphere, and is more likely to be distributed about the tropopause (at 42 km) and above.
 The distinct drop in haze opacity below 30 km observed by Young et al.  is not readily tested with the analysis presented here. While clearing of aerosols by rainout may occur below 30 km, minor changes to the extinction profile (Figure 2d) produce results outside of the observational uncertainty, suggesting that the atmosphere at the south pole is not cleared up to 80 km [McKay et al., 2001].
 It's not clear what concentrates Titan's particles in Titan's southern tropopause. The particles that we witness lie above the daily cumuli that appear at Titan's south pole. These particles reside at altitudes similar to those observed at 2 μm [Bouchez, 2003] and at 0.7–1.0 μm (C. A. Griffith et al., Imaging temporal changes on Titan, submitted to Icarus, 2004). Potentially they are related to the discrete clouds and form from the same updrafts that may form the lower clouds. Another possibility is that they represent haze concentrated dynamically by Titan's circulation [Rannou et al., 2003]. Alternatively we may be observing the condensation of ethane on settling particles, which occurs above that of methane [Barth and Toon, 2003, 2004].
 As field integral spectrometers come online, it will be possible to regularly produce datacubes such as the one presented here for monitoring of the seasonal variations (29.5 year cycles) in the 3-dimensional spatial distribution of haze and clouds. Such information will be necessary to test models that couple circulation and the photochemical formation of aerosols on Titan. Remote observations will remain necessary to have a dynamical understanding of Titan's atmosphere, even after detailed measurements are made possible by the arrival of the Cassini spacecraft to Titan on its 4 year mission.
 The data were obtained at the W. M. Keck Observatory, which is operated as a scientific partnership among the California Institute of Technology, the University of California and the National Aeronautics and Space Administration. The Observatory was made possible by the generous financial support of the W. M. Keck Foundation. This particular study was partially supported by the National Science Foundation and Technology Center for Adaptive Optics, grant no. AST-0205893, managed by the University of California at Santa Cruz under cooperative agreement No. AST-9876783.