© ESO, 2015

1. Introduction

The dwarf planet (1) Ceres is the only one in the inner solar system. It probably represents a unique remnant of the primordial population of large planetesimals that were removed later on by dynamical mechanisms, thus depleting the asteroid main belt of most of its original mass (e.g., Morbidelli et al. 2009). The modeling of the thermo-physico-chemical evolution of Ceres, which is constrained by the available shape and density measurements (2077 ± 36 kg m^-3, Thomas et al. 2005; 2206 ± 43 kg m^-3, Carry et al. 2008), points to a differentiated interior. This probably consists of an inner core made of dry silicates, an outer layer made of hydrated silicates, and an outer shell of water ice (Castillo-Rogez & McCord 2010). Alternatively, an undifferentiated porous interior, consisting of a mixture of hydrated silicates, has been proposed (Zolotov 2009). Both the albedo (0.090 ± 0.003, Li et al. 2006) and the visible and near-infrared spectra of Ceres are similar to those of carbonaceous chondrites, and evidence for aqueous alteration has been found.

The presence of surface water ice on Ceres, possibly resupplied from the mantle through fractures in a silicate and ice crust, has been debated at length (see Rivkin et al. 2011, for a review of Ceres’ surface composition). So far, rotationally resolved spectra of Ceres (P = 9.074170 ± 0.000002 h, Chamberlain et al. 2007) were acquired in the near-infrared region by Rivkin & Volquardsen (2010) and Carry et al. (2012), who report evidence for a relatively uniform surface. Before the present study, no study of visible spectra variation with the Ceres’ rotation had been performed. Recently, Küppers et al. (2014) have identified two localized sources (~60 km in diameter) of water vapor on Ceres at planetocentric longitudes corresponding to the dark regions Piazzi (long. 123°, lat. +21°) and Region A (long. 231°, lat. +23°). It has been suggested that water outgassing is due to comet-like sublimation or to cryo-volcanism.

In this work we analyze new visible and near-infrared spectra of Ceres obtained at different rotational phases, in order to enhance our knowledge of its surface composition. We also review the interpretation of the 3-μm feature observed in Ceres’ spectra by different authors. Our results can be useful for supporting the NASA Dawn mission (Russell et al. 2004), which will start orbiting Ceres in March 2015.

2. Observations and data reduction

Observations were carried out at the 3.6-m Telescopio Nazionale Galileo (La Palma, Spain) during two runs (December 2012, and January 2013). The observational circumstances are given in Table 1. Visible spectroscopy was performed with the DOLORES instrument using the low-resolution blue (LR-B) and red (LR-R) grisms. Near-infrared (NIR) data were taken with the NICS instrument coupled with the Amici prism, in low-resolution mode. NIR observations were carried out using the standard nodding technique of moving the object along the slit between two positions A and B. Each of the two NICS spectra that we present was obtained from one ABBA sequence. For both visible and NIR ranges, spectra were taken through a 2′′ slit, oriented along the parallactic angle to avoid flux loss due to the differential refraction.

Data were reduced with the software package ESO-Midas, using standard procedures (e.g., Fornasier et al. 2004): for the visible data: subtraction of the bias from the raw data, flat field correction, cosmic rays removal, background subtraction, collapsing the two-dimensional spectra into one dimension, wavelength calibration (using Ar, Ne+Hg, and Kr lamps’ emission lines), and atmospheric extinction correction. NIR data were corrected for flat field, A-B and B-A pairs were subtracted, the four different frames were shifted and added, then the spectrum was extracted. Wavelength calibration was obtained using a look-up table, available on the instrument website, which is based on the theoretical dispersion predicted by ray-tracing and adjusted to best fit the observed spectra of calibration sources. The reflectivity of Ceres was then obtained by dividing its visible and NIR spectra by those of solar analogs observed close in time and in airmass to the scientific frames (cf. Table 1).

The resulting visible and NIR spectra are presented in Figs. 1 and 2, respectively. During each of the two observing runs, we obtained three complete spectra of Ceres with the LR-B + LR-R grisms (covering the 0.44–0.81 μm and 0.54–0.9 μm wavelength ranges, respectively). The planetocentric coordinates for each observation (Table 1) were calculated using the IMCCE webtools (Berthier et al. 2008), according to the pole solution by Carry et al. (2008). Two NIR spectra were also acquired during the December 2012 run.

	Fig. 1 Visible LR-B (black) and LR-R (orange) spectra of Ceres, shifted by 0.15 in reflectance for clarity. The LR-B spectrum #6 has been cut at 0.7 μm because affected by a poor sky subtraction longward.
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	Fig. 2 NIR spectra of Ceres, shifted by 0.1 in reflectance for clarity. Regions affected by strong atmospheric absorption have been cut out.
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3. Data analysis and results

The two NIR spectra we obtained do not show significant variations, in agreement with Carry et al. (2012). Though noisy and of low resolution, both of them show the very broad absorption centered at ~1.2 μm already observed on Ceres, as well as on several carbonaceous chondrites, and interpreted as possibly due to magnetite or plagioclase feldspar (Rivkin et al. 2011).

The visible spectra obtained from the six simultaneous LR-B and LR-R observations show a very good agreement between the two grisms, making us confident about the goodness of our results. In Table 1 we report the spectral slope computed in the 0.55–0.8 μm range, considering the LR-B and LR-R data together. Figure 3 shows the obtained spectral slopes as a function of the longitude of the subobserver point. A variation through the rotational phase is evident, whose amplitude is about one order of magnitude greater than that reported for NIR observations (Carry et al. 2012). We also stress that, while all of the spectra taken in January 2013 (phase angle ~13.5°) are redder than those acquired in December 2012 (phase angle ~0.7°), the observed variations are about two orders of magnitude greater than those that could be introduced by the phase reddening effect (e.g., Sanchez et al. 2012).

While we cannot determine the exact cause of these variations (possibly due e.g. to different composition, albedo, geological features, surface age), we stress that the spectra #3 and #5 – as well as, to a minor extent, #1 and #4 – sample the same regions on the surface, observed one month apart, and present a significant variation in the slope (~2–3%/10³ Å). Noteworthy is that our observing runs (December 2012 and January 2013) are temporally encompassed by the water vapor detections around Ceres (October 2012 and March 2013) performed with the Herschel Space Observatory by Küppers et al. (2014). We therefore guess that the observed variation in the visible spectral slope could be linked with the resurfacing after outgassing episodes. The bluer spectrum could correspond to larger quantities of exposed water ice and/or some “B-type” asteroidal material (possibly exposed and/or redeposited by water sublimation). The redder spectrum could instead be tentatively associated with more exposed organics: though these have not been yet clearly detected, their presence on Ceres – as for water ice – is considered likely based on thermo-physical considerations (Castillo-Rogez & McCord 2010), and they could possibly lie in the near-surface environment (Rivkin et al. 2011). Moreover, a mix of water ice and organics has already been invoked to fit the Ceres’ 3-μm band (see next section). The much smaller slope variations observed by Carry et al. (2012) in the NIR could then be associated with periods of no/lower water activity by Ceres (e.g., Herschel did not detect the water vapor on November 2011), or the Ceres’ spectrum could be intrinsically less variable at NIR wavelengths than in the visible. Our spectra #2 and #6, acquired at planetocentric longitudes ~30° apart, show a slope variation similar to what was previously reported for the NIR. This could strengthen the hypothesis of localized active regions on the surface of Ceres.

The existence and spatial extent on Ceres of a broad spectral feature around 0.6–0.7 μm, usually attributed to aqueous alteration products (e.g., saponite, Cloutis et al. 2011), is still open to debate (Rivkin et al. 2011). To verify the presence and variability of such absorption in our spectra, we removed the continuum computed as a linear fit to each spectrum in the region 0.55–0.8 μm. A very faint feature (0.5–0.7%) centered at ~0.67 μm seems present in spectra #1 and #2 for both LR-B and LR-R grisms. No noticeable absorption is identified in our other spectra, maybe only because of lower S/N (Table 1 and Fig. 4).

	Fig. 3 Visible spectral slope (0.55–0.8 μm) vs. planetocentric longitude. Data from Dec. 2012 (dots) and Jan. 2013 (asterisks).
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For comparison, we also reanalyzed the few visible spectra of Ceres available in the literature, computing the spectral slope and looking for the presence of the aqueous alteration band (Table 2). An absorption centered at 0.67 μm and with depth 1.7% is clearly seen in the spectrum by Vilas et al. (1993). The spectrum from Vilas & McFadden (1992) seems to exhibit two superimposed features with minima at 0.6 μm and 0.67 μm, with an overall depth <1.0%, though the double minimum could be an artifact attributable to poor S/N. A similar result is found for the spectrum by Fornasier et al. (1999), while no feature is seen in the data by Bus & Binzel (2002) and Lazzaro et al. (2004). As for the spectral slope, we note that the magnitude of its variation is not as prominent in the literature data as in our dataset, despite the uncertainties from the different observing conditions and techniques, the instrumentation, etc.

	Fig. 4 Continuum-removed LR-B and LR-R spectra #1 and #2 (shifted by 0.05 in reflectance for clarity), with a superimposed polynomial fit.
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4. The 3-μm band and the water ice on Ceres

A broad 3-μm feature was observed on Ceres for the first time by Lebofsky (1978) and associated with the presence of clay minerals containing water of hydratation. Analyzing higher spectral resolution data, the 3-μm band was confirmed by Lebofsky et al. (1981), who also found a relatively narrow absorption centered near 3.06 μm, which was interpreted as due to a very thin layer of water ice frost. This feature, along with a set of overlapping bands at 3.3–3.4 μm, was reinterpreted by King et al. (1992) as due to ammoniated phyllosilicates. Vernazza et al. (2005) revisited ice as an explanation, reproducing the 3.06-μm feature with a linear combination of crystalline water ice and an organic component, the residues of ion-irradiated asphaltite covered with water ice. Rivkin et al. (2006) furthermore reinterpreted the 3.06-μm band as due to an iron-rich clay (the serpentine cronstedtite) and the 3.3–3.4 and 3.8–3.9 μm bands as caused by carbonates. The same dataset was then modeled by Milliken & Rivkin (2009) to identify the 3.06-μm band as brucite (Mg(OH)₂) and confirm the presence of carbonates. Beck et al. (2011) propose impure goethite (FeO(OH)) as an alternative origin of the 3.06-μm band, though Jewitt and Guilbert-Lepoutre (2012) stress that goethite, when found in meteorites, is a product of aqueous alteration in the terrestrial environment and that extraterrestrial goethite in freshly fallen meteorites is unknown.

	Fig. 5 Up: Ceres’ 3-μm spectra taken in 1987 (Jones et al. 1990), 2004 (Vernazza et al. 2005), 2005 (Rivkin et al. 2006). Down: the 2004/2005 spectral ratio and the spectrum of crystalline (150 K) water ice.
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In Fig. 5 we show the 3-μm region spectra by Jones et al. (1990), Vernazza et al. (2005), and Rivkin et al. (2006), acquired in 1987, 2004, and 2005, respectively. In the first two works, the presence of the 3.1-μm absorption due to crystalline water was claimed. In Fig. 5 we also show the ratio of the high-resolution 2004/2005 spectra, as well as a laboratory spectrum of crystalline (150 K) water ice (Strazzulla et al. 2001). Supposing that the 3-μm band is composed of two components, as suggested by Vernazza et al. (2005), the ratio of the two spectra may reveal a change in the relative abundances. Indeed, the ratio of the spectra from 2004 and 2005 is very similar to the spectrum of crystalline water, with a minimum at ~3.1 μm. The absorption starting at 3.15 μm in the 2004 spectrum is due to the terrestrial atmosphere, as stated by Vernazza et al. (2005).

Following our findings about the short-term temporal variation of the visible spectral slope, as well as the recent identification of localized emission of water vapor around Ceres, we suggest that the shape of the 3-μm band could also change in time: i.e., Vernazza et al. (2005) could have really observed crystalline water ice, while Rivkin et al. (2006) could have observed Ceres when surface ice was less abundant and not detectable.

5. Summary and conclusions

The new visible and NIR spectra that we analyze in this work are generally compatible with the previous data of Ceres.

The feature at 0.67 μm seen in previous observations (e.g., Vilas et al. 1993), and interpreted as due to aqueous alteration, is possibly observed in two out of our six visible spectra (those with higher S/N), although the measured band depth is very small (0.5–0.7%). Data taken in December 2012 and January 2013 show a clear variation in the visible spectral slope: at longitudes ~25° and ~270° we measure a slope difference of (3.2 ± 1.0)%/10³ Å and (2.4 ± 0.7)%/10³ Å, respectively. Such variations are much more important than those already reported in the literature, and they strongly point towards a variable character of the Ceres’ surface. While the regions we identified (which are however approximate due to our disk-integrated observations) do not correspond with those detected as emitting water vapor by Küppers et al. (2014) in October 2012 and January 2013, we can hypothesize that Ceres was undergoing extended resurfacing processes (due to cryovolcanism or cometary activity) during that period. These new results also lead us to propose a coherent and reconciling solution for the disagreements in the literature about the shape and interpretation of the 3-μm band, which could change in time according to the different quantity of exposed water ice. The NASA Dawn mission that will start to orbit Ceres in March 2015 will hopefully provide key information about the surface variegation and any outgassing activity of Ceres.

Acknowledgments

We thank A.S. Rivkin and P. Vernazza for kindly providing their spectral data. The research of Z.K. is supported by VEGA – The Slovack Agency for Science, Grant No. 2/0032/14. This program was supported by the French national space agency CNES and French INSU – PNP program.

References

Online material

Appendix A: About the solar analog stars

	Fig. A.1 Spectral ratios of the three solar analog stars observed during the night of 18–19 Dec. 2012. The airmasses at the moment of the acquisition are reported.
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	Fig. A.2 Spectral ratios of the three solar analog stars observed during the night of 18–19 Jan. 2013. The airmasses at the moment of the acquisition are reported.
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To verify that the observed variability of Ceres’ visible spectra is real, and not an artifact of the different solar analog stars used for calibration, we divided each by all the others to check that this results in a flat spectrum. We considered the LR-R spectra in the same wavelength range used for computing the Ceres’ visible spectral slope, 0.55–0.8 μm. Figures A.1–A.3 show the relative ratios of the three solar analog stars observed during each night, on 18–19/12/2012, 18–19/1/2013, and 19–20/1/2013. For the second of these nights (Fig. A.2), the stars were observed at low airmass and their spectral ratios are flat (slopes of −0.02 ± 0.15%/10³ Å and 0.10 ± 0.18%/10³ Å). The spectral ratios of stars observed during the other two nights present a slightly positive slope (≲0.5%/10³ Å), which is probably due to the higher airmasses involved. The obtained flat behavior makes us confident about the reliability of our results. As for the first of our observing nights (17–18/12/2012), we do not have other solar analogs to compare with the one used to obtain the Ceres’ reflectance; however, Fig. A.4 shows that its division by a solar analog observed the following night still presents a flat spectrum. The same result is found when dividing the spectra of two solar analog stars observed during the two different nights we had in January 2013, as well as when dividing two solar analog stars whose spectra where acquired in December 2012 and January 2013. All of these ratios show some telluric features, which are of course natural because of the different observing conditions (why all of the Ceres’ spectra have been calibrated using a star observed close not only in airmass but also in time) and do not affect the overall spectral slope. The above strongly suggests that the slope variability we present in this work is indeed due to some short-term processes acting over the surface of Ceres.

	Fig. A.3 Spectral ratios of the three solar analog stars observed during the night of 19–20 Jan. 2013. The airmasses at the moment of the acquisition are reported.
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	Fig. A.4 Spectral ratios of solar analog stars observed during different nights. Night 1 = 17–18 Dec. 2012, Night 2 = 18–19 Dec. 2012, Night 3 = 18–19 Jan. 2013, Night 4 = 19–20 Jan. 2013.
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Appendix B: About a possible link between ours and Herschel’s observations

The likely sources of the water vapor detected by the Herschel Space Observatory are two 60-km wide dark regions centered at long. 123°, lat. +21°, and long. 231°, lat. +23°. In this work we report a temporal spectral variability of Ceres, for nearly equatorial observations centered at planetocentric longitudes ~25° and ~270°, and suggest that this could be associated with variable amounts of exposed water ice. One could object that it is difficult to explain why such longitudes do not coincide, given that ours and Herschel’s observations were made in the same timeframe, and we propose that the spectral changes could be related to outgassing episodes like those seen by Herschel. Moreover, it would be difficult to imagine that the slope changes we measured are provoked by such small active areas. In this regard, we stress that i) our spectra are disk-integrated, so it is basically impossible to state where the water ice could lie exactly on the observed surface. ii) The Herschel telescope detected water vapor, while we suggest the presence of water ice on the surface. Küppers et al. (2014) suggest two dark regions as likely sources of most of the evaporating water, because these are warmer than the average surface, resulting in efficient sublimation of possible water ice reservoirs. The water ice we observe could be more concentrated in other regions of the surface, where dark (hotter) material is less abundant and/or at higher latitudes where sublimation could be slower. iii) The 60-km size estimated in Küppers et al. (2014) is somewhat model-dependent: varying the involved parameters (e.g., the mixing ratio of active/inactive components and its spatial variation over the surface), one can change the size of the “most active” spots. iv) Our observations performed in December 2012 show bluer spectra (i.e., more water ice following our assumption) than in

January 2013. Herschel clearly detected water in October 2012, whereas in March 2013 the emission line was much weaker. As a result, both the datasets could suggest a decreasing quantity of exposed water ice from late 2012 to early 2013.

Appendix C: About the 3-μm band variation

Rivkin & Volquardsen (2010) saw variations of a few percentage points over Ceres’ surface. Since the Rivkin et al. (2006) spectrum is an average over the entire rotational period of Ceres, while the Vernazza et al. (2005) spectrum covers a smaller portion of the surface, it may be that the spectrum did not change at the longitude of the Vernazza observations. While we cannot exclude such a possibility, it would imply that Rivkin et al. (2006) were wrong in excluding the presence of water ice. Here we suggest that water ice is indeed present on the surface of Ceres. Its superficial abundance could be variable and concentrated in particular (colder) regions. We hope that the Dawn mission will clarify this issue, even though it will arrive at Ceres post-perihelion, when the heliocentric distance (around 2.9 AU) will not be favorable for detecting cometary-like activity.

All Tables

All Figures

	Fig. 1 Visible LR-B (black) and LR-R (orange) spectra of Ceres, shifted by 0.15 in reflectance for clarity. The LR-B spectrum #6 has been cut at 0.7 μm because affected by a poor sky subtraction longward.
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In the text

	Fig. 2 NIR spectra of Ceres, shifted by 0.1 in reflectance for clarity. Regions affected by strong atmospheric absorption have been cut out.
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In the text

	Fig. 3 Visible spectral slope (0.55–0.8 μm) vs. planetocentric longitude. Data from Dec. 2012 (dots) and Jan. 2013 (asterisks).
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In the text

	Fig. 4 Continuum-removed LR-B and LR-R spectra #1 and #2 (shifted by 0.05 in reflectance for clarity), with a superimposed polynomial fit.
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In the text

	Fig. 5 Up: Ceres’ 3-μm spectra taken in 1987 (Jones et al. 1990), 2004 (Vernazza et al. 2005), 2005 (Rivkin et al. 2006). Down: the 2004/2005 spectral ratio and the spectrum of crystalline (150 K) water ice.
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In the text

	Fig. A.1 Spectral ratios of the three solar analog stars observed during the night of 18–19 Dec. 2012. The airmasses at the moment of the acquisition are reported.
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In the text

	Fig. A.2 Spectral ratios of the three solar analog stars observed during the night of 18–19 Jan. 2013. The airmasses at the moment of the acquisition are reported.
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In the text

	Fig. A.3 Spectral ratios of the three solar analog stars observed during the night of 19–20 Jan. 2013. The airmasses at the moment of the acquisition are reported.
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In the text

	Fig. A.4 Spectral ratios of solar analog stars observed during different nights. Night 1 = 17–18 Dec. 2012, Night 2 = 18–19 Dec. 2012, Night 3 = 18–19 Jan. 2013, Night 4 = 19–20 Jan. 2013.
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In the text