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Article

Laboratory Emissivity Spectra of Sulphide-Bearing Samples, New Constraints for the Surface of Mercury: Oldhamite in Mafic Aggregates

by
Cristian Carli
1,*,
Sabrina Ferrari
2,
Alessandro Maturilli
3,
Giovanna Serventi
4,
Maria Sgavetti
4,
Arianna Secchiari
4,5,
Alessandra Montanini
4 and
Jörn Helbert
3
1
National Institute for Astrophysics (INAF), Institute for Space Astrophysics and Planetology, Via Fosso del Cavaliere 100, 00133 Roma, Italy
2
Department of Geoscience, University of Padova, Via Gradenigo 6, 35131 Padova, Italy
3
German Aerospace Center (DLR), Institute for Planetary Research, Rutherfordstraße 23, 12489 Berlin, Germany
4
Department of Chemistry, Life Science and Environmental Sustainability, University of Parma, Parco Area delle Scienze, 11/a, 43124 Parma, Italy
5
Department of Earth Science “A. Desio”, University of Milan, Via Botticelli 23, 20131 Milano, Italy
*
Author to whom correspondence should be addressed.
Minerals 2024, 14(1), 62; https://doi.org/10.3390/min14010062
Submission received: 25 September 2023 / Revised: 18 December 2023 / Accepted: 28 December 2023 / Published: 4 January 2024
(This article belongs to the Special Issue VNIR-TIR Spectroscopy: How Reflectance and Emissivity of Minerals, Rocks and Meteorites Can Help Planetary Exploration)
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Abstract

:
Exploration of Mercury will continue in the near future with ESA/JAXA’s BepiColombo mission, which will increase the number and the type of datasets, and it will take advantage of the results from NASA’s MESSENGER (MErcury Surface, Space ENviroment, GEochemistry and Ranging) mission. One of the main discoveries from MESSENGER was the finding of a relatively high abundance of volatiles, and in particular of sulphur, on the surface. This discovery correlates well with the morphological evidence of pyroclastic activity and with features attributable to degassing processes like the hollows. BepiColombo will return compositional results from different spectral ranges and instruments, and, in particular, among them the first results from the orbit of emissivity in the thermal infrared. Here, we investigate the results from the emissivity spectra of different samples between a binary mixture of a volcanic regolith-like for Mercury and oldhamite (CaS). The acquisitions are taken at different temperatures in order to highlight potential shifts due to both mineral variation and temperature dependence on these materials that potentially could be present in hollows. Different absorption features are present for the two endmembers, making it possible to distinguish the oldhamite with respect to the regolith bulk analogue. We show how, in the mixtures, the Christiansen feature is strongly driven by the oldhamite, whereas the Reststrahlen minima are mainly dominated by mafic composition. The spectral contrast is strongly reduced in the mixtures with respect to the endmembers. The variations of spectral features are strong enough to be measured via MERTIS, and the spectral variations are stronger in relation to the mineralogy with respect to temperature dependence.

1. Introduction

The Hermean surface has been characterized, from a compositional point of view, mainly thanks to some element ratios measured during the MESSENGER mission via XRS (X-ray spectrometer; [1,2]) and GNRS (gamma ray and neutron spectrometer; [3,4]). Visible to near-infrared (VNIR) data, acquired by MESSENGER, show a large variability of spectral properties; however, they do not permit us to retrieve major mineralogical phases. Neither MASCS (Mercury stmospheric and surface composition spectrometer; [5,6]) nor MDIS (Mercury dual imaging system; [7,8]) spectra show diagnostic absorption, with the exceptions of rimless depressions with flat floors, called hollows, where MDIS colour images can reveal a potential absorption band, with a minimum between 630 and 750 nm. This minimum has been ascribed as related to the presence of either some sulphide, e.g., CaS, MgS or MnS [9,10], or to some iron-free mafic minerals [11] that contain alternative transition elements (e.g., Cr, Ti, Ni).
In particular, the possible presence of sulphide within hollows is intriguing considering that:
The hollows were morphologically attributed to degassing processes (e.g., [12,13]); relatively unexpected high S/Si has been measured on Mercury’s surface (e.g., [1,14]); the surface of Mercury has undergone extensive pyroclastic activity (e.g., [15,16,17,18]) which indicates high levels of volatile components in the magma reservoir [19].
In particular, in some specific regions where the level of S/Si is high, Mg/Si and Ca/Si also show higher values, suggesting the possible formation of CaS and MgS phases [1,20]. These sulphides have been observed in reflectance and emittance, suggesting potential spectral variation in the VNIR after different temperature cycles [10], though emissivity spectra of CaS (oldhamite) are not affected by Mercury’s surface condition, retaining their characteristic absorption features for both fresh and heated CaS samples [21]. Recently, ref. [22] reported the results about the thermal stability of CaS under Hermean temperature conditions.
The main mineralogy retrieved from elementary information suggests a volcanic composition with variable abundance of plagioclase (oligoclase-andesine), olivine (forsteritic) and pyroxene (enstatitic) (e.g., [23]). This possibly supports the hypothesis that regolith could be mainly characterized by rocks similar to terrestrial magnesian basalts, komatiite or boninite (e.g., [24,25,26]) with a much lower iron abundance (<1%, e.g., [27,28]) and a relatively higher albite content in plagioclase. The presence of higher iron abundance, or the presence of different transition elements, and/or differences in valence state in silicates, have a direct impact on VNIR spectral properties. In fact, VNIR reflectance properties are strongly influenced by electronic absorptions which often dominate the optical properties. On the other hand, in thermal infrared (TIR) emittance spectra, molecular absorptions provide mineralogical information, whereas transitional elements have a minor impact on Reststrahlen band positions (e.g., [29,30]). These variations do not impact the spectral shape of absorptions which are defined by vibrational processes within the crystal structure (e.g., [31,32]).
Plagioclase TIR spectra can vary from albite to anorthite endmembers [33], whereas the variation is smaller between An20 to An60 [34,35]. Nevertheless, the Na content in plagioclase has been retrieved in [23], taking into account the retrieved high Na2O (i.e., up to 7%) from [36] which was calculated from the Na/Si reported in [37]. This value has been measured for the north pole with GNRS, at relatively low spatial resolution, and this increase of Na/Si could be related to the migration of Na from the equatorial regions towards the poles [37]. Thus, other regions could have plagioclase with higher Ca composition, but even the retrieved albitic composition of plagioclase on northern lavas could be affected by Na/Si values that are not related to plagioclase [37].
The ongoing ESA/JAXA BepiColombo mission has an onboard VIHI (visible hyperspectral imager, [38], part of the SIMBIO-SYS, Spectrometer and Imaging for MPO Bepicolombo Integrated Observatory SYStem, experiment, [39]), that will acquire imaging data in a larger spectral (0.4–2.0 μm) range with respect to MESSENGER MDIS and MASCS. Moreover, spectral properties of the surface will be investigated using MERTIS (Mercury radiometer and thermal infrared spectrometer, [40]) which will acquire emissivity images in the TIR spectral range (7–14 μm).
The acquisition of spectral data of the surface in the TIR range will permit us to obtain mineralogical information assignable to molecular absorptions and thus recognise the different mineral phases present on the surface of Mercury from the cation–anion and lattice vibrations of crystalline structures in the middle portion of the electromagnetic spectrum (e.g., [31]).
To support the interpretation of future MERTIS data, in the last decade, emissivity spectra of single mineral phases (e.g., [21,30,41]) as well as spectra of rocks (e.g., [42,43,44]) were largely investigated at the PSL (Planetary Space Laboratory of DLR, [45]) at variable temperatures. These works highlighted the contribution of temperature variations on driving the shift of specific parameters, like Christiansen feature (CF) and, in particular, some Reststrahlen band absorption minima (RB). Such shifts may mimic variations in composition (e.g., [30]), thus highlighting the importance of taking into account the function of temperature on spectral variations.
Studying controlled and systematic mineral variations can reveal possible trends that can depend both on mineral associations and temperature, but there are few comprehensive studies on emissivity of mineral mixtures. The spectral analysis of mineral mixtures could also provide detection limits of the retrieved minerals. Recently, ref. [46] explored the variation of emissivity features of binary mixtures of plagioclase and clinopyroxene that underwent different temperatures. The authors show how the CF tends to shift to higher wavenumbers with increasing temperature and to lower wavenumbers with decreasing polymerization. Moreover, with increasing temperatures, the RBs shift their position and deepen with respect to CF emissivity, and at high temperatures the plagioclase’s higher-wavenumber RBs are not detected. This makes the plagioclase detection in that spectral range more complicated. At lower wavenumbers, a correlation between the pyroxene content and a specific absorption was observed, suggesting that shifts are driven by the pyroxene, which has higher expansion coefficient with respect to that of the plagioclase.
In this manuscript, we investigate the TIR spectral properties of the mineral mixture of a Mg-rich gabbronorite, representing a potential mafic mineralogy in terms of pyroxene-olivine-plagioclase abundances, and CaS, which could be a possible sulphide associated to the degassing processes on Mercury.

2. Methods

2.1. Selection and Preparation of the Samples

We prepared two different endmembers:
A mafic analogue represented by a Mg-gabbronorite (hereafter Mg-GN) from [47] mainly constituted by plagioclase (~62 vol.%), clinopyroxene (~16 vol.%), orthopyroxene (~11 vol.%) and olivine (~11 vol.%), with the mafic mineralogy being particularly Mg-rich; this sample was already used as mafic endmember mixed with graphite for VNIR reflectance acquisitions [48].
CaS has already been used in VNIR [10] and in MidIR [21] acquisitions as a potential Mercury analogue, as suggested from X-Ray (e.g., [1]) and VNIR data (e.g., [9,11]); CaS was chosen because, among the suggested sulphides, it remained stable on Mercury’s surface conditions [21,22].
Samples were reduced to <63 µm grainsize via multiple steps of sieving, in order to limit the amount of very fine sized (e.g., <5–10 µm) particles in the powder.
We produced 3 different mixtures, weighing the abundance of the two endmembers, Mg-GN and CaS, in 80%–20%, 60%–40% and 40%–60%, respectively, and preparing 3 g. per sample for emissivity measurements. This sample preparation was carried out at the Sample Preparation Facility at IAPS-INAF.
Sample cups were then prepared at the PSL a week in advance and placed in a desiccator cabinet.

2.2. Experimental Setup

Emissivity spectral measurements were performed at the PSL using a Bruker Vertex 80 V FTIR spectrometer. The set-up operates under low vacuum, with a liquid nitrogen-cooled HgCdTe detector and KBr beam splitter. Emissivity spectra were acquired between 9996 and 400 cm−1 at a spectral resolution of 4 cm−1. We then worked in the 2000–700 cm−1-range (5–14 μm), which is the most promising for diagnostic spectral features. The emissivity spectra of CaS were compared to data from [21] to investigate possible differences which could suggest sample’s weathering during the time. The spectra show negligible variations.
An externally evacuated planetary simulation chamber was used to measure emissivity (see [46] and references therein). Samples were heated once, and emissivity was measured under low vacuum at 0.7 mbar in subsequent steps at 375 K, 475 K, 575 K and 675 K. The cup height exceeded the sample height, ensuring more efficient heating and reducing the sample thermal gradients. For each measured sample, the final spectrum was a 256 averaged datum. To calibrate the emittance the calibration body (CB hereafter) was heated and measured at the same temperatures of the sample.
The sample radiance, I(T), and the CB radiance, CB(T), were collected at each scheduled step of temperature. For each sample, 5 scans were averaged to produce a single spectrum. The absolute emissivity of the sample εa(T) was derived using the εa(T) = I(T)/CB(T) · ECB, where ECB is the calibration body emissivity curve. More details regarding the calibration technique are discussed in [41].

2.3. Analytical Approach

Here, we describe the influence of the simulated environment on the measured spectra in terms of wavenumber position of the more diagnostic features and in terms of their spectral contrast.
We identified here different spectral signatures for the two endmembers in the 700–2000 cm−1 range. Then, since it is known that, in particular, in the 700–1400 cm−1 range, the Christiansen feature (CF) wavenumber and the spectral contrast between CF and the first group of absorption bands is strongly affected by thermal gradients occurring at the shallower radiative depths (see [46]), we concentrated in this range the spectral analysis.
In addition to the CF, the following emissivity minima are considered diagnostic parameters: (i) Reststrahlen bands (hereafter referred as RB) attributable to Si-tetrahedral fundamental vibrations [49] and (ii) transparency features (hereafter referred to as TF) caused by the volume scattering characteristic of fine particle sizes [50]. RBs have long been identified as diagnostic of composition (e.g., [49]) and their frequencies are unaffected by thermal gradients.
Since measurements do not show any evident TF, we just consider CF and RBs positions numbered following the Mg-GN order from highest to lowest wavenumber, as well as the spectral contrast (SC or relative intensity) between the CF and RBs minima, similarly to [46]. Those parameters are discussed with respect to the temperature variation and function of the Mg-GN (mafic endmember) content.

3. Results

At 375 K, the mafic endmember Mg-GN showed the maximum emissivity, i.e., the CF, at 1229 cm−1, consistent with the bulk mafic composition ([51], and references therein) of this sample (see Figure 1, black line, and Table 1, where the data for the lowest temperature, 375 K, are summarized). The RB absorption was composed of 5 different minima of emissivity at 1113, 1001, 959, 928 and 876 cm−1, hereafter indicated as RB0, RB1, RB2, RB3 and RB4, respectively. RB0 was only evident in the Mg-GN endmember (see Table 1), whereas all of the other minima were evident for all the mixtures (see Figure 1 and Figure 2). Additionally, we report the presence of two other maxima (dark blue thin arrows in Figure 1) at ~1080 cm−1 and at 780 cm−1, which enclose the RB from 1 to 4.
The other endmember, CaS, instead showed a maximum in emissivity at 1099 cm−1 (CF, Table 1), reported also as 9.1 μm in [21]. This mineral phase showed three absorptions at 1038, 885 and 837 cm−1, reported hereafter as RB1*, RB4* and RB5, respectively (see Figure 2, bottom plot). RB1* and RB4* are very close to mafic minima RB1 and RB4, and so in the mixtures, their parameters will be compared to the mafic minima. In Table 2 and Table 3, we reoprt the data at different of temperatures, for band position, emissivity and band contrast.
In Figure 1, we also highlighted the presence of two well-defined peaks at 1510 and 1430 cm−1, respectively. The next absorptions, at slightly lower wavenumbers, are indicated as B1 and B2. This portion of the spectral range has not been considered in previous works, though they show specific features of CaS. The maxima (peaks, Max B1 and Max B2 in Table 4), in particular, rose even with a low quantity of sulphides in the mixture (20% of sulphides, dark grey in Figure 1), though they were superimposed by the mafic background already at 60% sulphides, as indicated by the mafic wide weak peak around 1600 cm−1. Nevertheless, they occurred at wavenumbers higher than those covered by MERTIS, so we will not discuss the different temperatures in the rest of the manuscript.
Two absorptions (B3 and B4) were also present at ~1200 and 1120 cm−1, at wavenumbers higher than the CaS CF but lower than the mafic CF and closer to the weak RB0.
The CF and the absorption minima positions of emissivity spectra collected at 475, 575 and 675 K are listed in Table 2. Diagnostic features of measured emissivity spectra are listed in terms of CF locations and absorption-band minima positions. In Table 3, we report the spectral contrast of each absorption with respect to the emissivity of the CF.
Figure 2 shows the variation of emissivity in the spectral range from 1429 to 714 cm−1 for each sample at different temperatures. The emittance at the CF of the two endmembers was coincident for all the different temperatures (see Table 3 and Figure 2). Likewise, the CF position did not shift for Mg-GN (see Table 1 and Table 2 and Figure 2), whereas for CaS a shift at lower wavenumber from 1099 to 1085 cm−1 moving from 375 K to 675 K was observed. With increasing temperature, both endmembers showed a decrease of emissivity at wavenumbers lower than CF. All the mixtures showed a decrease of emittance from the lower temperature up to higher temperature for the entire spectral range (see Figure 2 and Table 3).
Moreover, we detected a shift of the CF at wavenumbers closer to those of the CaS endmember (evident also in Figure 1 for 375 K, Figure 2 for the other temperatures and in Figure 3) for all the mixtures. In particular, the CF of the 20% CaS sample was at a lower wavenumber with respect to that of the sulphide endmember. In contrast, with an increase of the CaS content in the mixtures, the CF moved closer to the correspondent endmember (see Figure 3). This behaviour is not linear, and it is influenced by the presence of the second maximum of the Mg-GN, which separates the RB0 from the rest of the RB minima (see Figure 1 and Figure 2).
RBs 1–4 were always present (apart from in the CaS spectra), giving a clear indication of the mafic components up to at least 60% CaS, conversely from CF. RB1 and RB3 were those moving more systematically from the wavenumber of Mg-GN up to the wavenumbers of RB1* and RB4* with increases to both the percentage of CaS and the temperature (Figure 4). RB1 moved from 1001 to 1018 cm−1, increasing the wavenumber for Mg-GN to 60% CaS (Figure 5a,c), whereas RB3 moved from 928 to 910 cm−1, decreasing the wavenumber (Figure 5b,d). RB2 instead was strongly diagnostic, since it showed a weak shift (Figure 4), 8 cm−1 lower than that which appears for Mg-GN and for all the mixtures. In fact, it showed the highest shift with the temperature for the endmembers itself (from 959 cm−1 at 375 K up to 951 cm−1 at 675 K, see Table 1), and it showed the highest shifts with respect to all the samples at the highest temperature (from 951 cm−1 for Mg-GN up to 959 cm−1 for the 60% CaS; see Table 2) (Figure 5a,c). RB4 displayed a trend towards lower wavenumbers, since it moves from 876 cm−1 to 862 cm−1 increasing the CaS percentage (Figure 5b,d), despite the CaS is at ~1030 cm−1. The wider shift is present for the 60% CaS (the sample with the mafic material at lower wavenumber) up to RB4*, for all the temperatures. This is mainly attributable to the influence of RB5 in CaS (Figure 1 and Figure 2, Table 1 and Table 2), which is at 833–794 cm−1, varying the temperature.
In Figure 6, the spectral contrast (i.e., the differences between the CF emissivity and the absorption–minima emissivity; see also [46]) of RBs 1–4 is compared to temperature (upper panel) and composition (lower panel). Interestingly, the spectral contrast showed a very similar behaviour for all four RBs. It showed the highest values for the two endmembers and then, in general, moved from 60% CaS, 40% CaS and 20% CaS, for which it showed the lower spectral contrast (Figure 6 top panel). Moreover, the spectral contrast seemed to increase with increasing temperature, as it appears in Figure 2. Nevertheless, the increase with temperature was evident for the two endmembers for all the 4 RBs (Figure 6, below panel and Table 3), whereas it was not for the mixtures, showing how the mineralogical variations (in terms of percentage) of each endmember affect the spectral contrast too. Moreover, on average between the different temperatures, the value of spectral contrast from 20% CaS up to 60% CaS was almost identical. The variations in RB2 and RB3 were negligible (from 0.056 ± 0.015 up to 0.065 ± 0.014, and from 0.047 ± 0.016 up to 0.060 ± 0.016, respectively), whereas the slight increase for RB1 and RB4 (from 0.054 ± 0.011 up to 0.080 ± 0.008, and from 0.028 ± 0.016 up to 0.061 ± 0.017, respectively) was affected by the intensity of the CaS absorption (Figure 6, below panel).

4. Discussion

Oldhamite has been reported in meteorites [52,53], and its presence is also suggested for the Hermean surface (e.g., [1]). Moreover, oldhamite stability is demonstrated in highly reducing conditions [52] and at high temperatures [22]. On Mercury’s surface, CaS is possibly mixed with volcanic bedrock with mafic mineralogy enriched in Mg. Here, we analysed the MidIR emissivity properties of potential mixtures of oldhamite and a Mg-rich GN (Figure 1 and Figure 2), to investigate the future possibility of identifying them from BepiColombo remote sensing data.
The CF position had distinct values between the Mg-GN and the CaS, and it moved closer to the CF position of the CaS even for the 20% CaS sample (Figure 3). This clearly indicates that relatively low abundance of CaS within the regolith could be identified using TIR measurements. The presence of a secondary maximum in the Mg-rich mafic endmember within the Reststrahlen minima at wavenumber ~1070 cm−1, lower than the CF position of CaS, affected the shift. In fact, the CF showed a lower wavenumber position for the 20% CaS, and the CF wavenumber increased for higher CaS abundances. This could also help to distinguish, with MERTIS data, regions with low CaS with respect to those dominated by CaS.
The shift attributable to the temperature for each sample was much lower (~3 cm−1), indicating that any CF shift detected via MERTIS should be attributed to compositional variation. Nevertheless, the CF of CaS showed a shift of 14 cm−1, mainly moving from 575 K to 675 K (Table 1 and Table 2 and Figure 3). This shift, attributable to temperature, could also be detected via MERTIS, which has a resolution of 90 nm [35], which means a variation from 5 to 20 cm−1 [46].
Moving to lower wavenumbers, the RBs of mafic material showed 5 minima (RBs 0, 1, 2, 3 and 4) with four of them clearly identifiable also on the mixture spectra (RBs 1, 2, 3 and 4). RBs appeared at lower wavenumbers with respect to the CF. Three different minima are present in the CaS, closer to the position in mafic endmembers, reported as RBs 1*, 4* and 5. RBs 1, 2, 3 and 4 are identifiable for each sample bearing Mg-GN and for all the temperatures considered. This clearly indicates that the composition of the volcanic rocks present in the regolith could be clearly distinguished with RBs even for high abundance (at least 60%) of CaS, unlike the CF.
The positions of RBs 1, 3 and 4 were affected by the increasing abundance of CaS, with RB1 moving towards RB1* and RB3 and RB4 shifting towards RB4* and RB5, respectively. The shifts of the RBs seems to have been affected by the CaS’s properties. CaS has an expansion coefficient (αV) of 4.03 × 10−5 K−1 [22], which is higher than those related to the main silicates present on a typical volcanic rock, e.g., 2.2 × 10−5 K−1 for a plagioclase [54] or 2.7 × 10−5 K−1 for a clinopyroxene [41]. Similar to what was evidenced in [46], this behaviour seems to confirm that the minerals with higher expansion coefficient also drive the main RB shifts in the mixtures.
RB2 showed a relative smaller shift (from 959 to 951 cm−1 from 375 K up to 675 K, for Mg-GN); this indicates that RB2 was less influenced, with respect to the other RBs, by mineral mixing with CaS (Figure 4). Though RB2 showed a peculiar variation in function of the temperature, at 375 K, all the spectra had the same absorption position, which shows a shift towards lower wavenumber increasing the Mg-GN abundance at higher temperature (Figure 5), similar to those observed in [46].
The spectra showed, in general, decreasing emissivity with increasing temperature, in particular at wavenumbers higher than the CF (Figure 2), and the RBs seem to have had the same behaviour. Once we highlighted the behaviour of the apparent intensity (see Table 3 and Figure 6), the RBs became deeper only for the two endmembers Mg-GN and CaS spectra, with RBs deepening with increasing temperature, whereas within mixtures, the relative intensity of RBs is strongly reduced in 60% CaS, since for 20% CaS and 40% CaS it is negligeable. Interestingly, this demonstrates that varying the temperatures and taking into account endmembers with the same particle sizes, the variation in the spectral contrast is more effective for CaS than Mg-GN.

5. Conclusions

TIR measurements of the two endmembers considered in this work support the probable capability to detect the presence of oldhamite on the surface of Mercury with the BepiColombo MERTIS instrument, even if oldhamite is mixed with a Mg-enriched volcanic regolith. Endmembers and mixtures, in fact, show very different spectral properties, having CF at different wavenumbers and having different RBs. Furthermore, it is evident that certain features are predominantly influenced by one endmember or the other. In several cases, the variations in mineral abundance have a more pronounced impact than temperature shifts on these features.
In particular, the CF was strongly driven by the CaS; therefore, the 20% CaS mixture already showed a CF at wavenumbers closer to the CaS end-memeber. However, an interesting shift is also associated to the maxima between RB0 and RB1 in the Mg-GN. This shift is towards lower wavenumbers with respect to the two endmembers, which may help the oldhamite interpretation. In fact, a small shift of the CF from the expected position for the oldhamite could give an indication of a relatively low amount of oldhamite within a specific pixel.
Conversely, for all the mixtures investigated here, the RBs indicate the presence of the mafic Mg-GN endmember. Nevertheless, at least for three of them, RBs 1, 3 and 4, the presence of the CaS was effective, with shifts that went towards RB1*, RB4* and RB5, whereas RB2 showed a very reduced shift, which is important to quantify Mg-GN composition. Moreover, RB2 could permit us to differentiate regions where oldhamite can be present with respect to regions where it is negligible.
Emissivity as a function of temperature was mainly evident for the endmembers, with an RB–CF spectral contrast that increased with the temperature. In the mixtures, lower spectral contrast values occurred even if an asymmetrical variation with respect to the composition change was evident, indicating that oldhamite spectra show more intense absorption in the RB spectral region with respect to Mg-GN.
MERTIS laboratory performance showed signal-to-noise ratios greater than 200 in the 1000–1200 cm−1 range, indicating a noise level lower than 0.5% [55], and conservatively 1% for the entire spectral range [35]. Such performance of the instrument will permit us to demonstrate several of the features discussed here. Moreover, considering the spectral resolution of the instrument, the most prominent and diagnostic shifts due to the composition effects, also within the mixtures, will be highlighted, not only for the CF but also for RBs 1 and 3, with RB4’s maximum shift closer to the resolution, whereas the shifts due to the temperature within each feature are mainly lower than the spectral resolution, even if for some features, and in particular, for RB5, the temperature effects should be present.
We suggest that future studies should explore the range from 20% CaS down to 0% CaS (mafic endmember) to better highlight the variation in the spectra for lower CaS abundance than those explored in this work. In particular, this is expected to retrieve possible correlation lines for the CF, which could be pivotal to detect and quantify the CaS within the hollows as well as in the regolith.

Author Contributions

Conceptualization, C.C., A.M. (Alessandro Maturilli) and G.S.; Methodology, C.C., S.F., A.M. (Alessandro Maturilli) and G.S.; Formal Analysis, C.C., G.S. and S.F.; Investigation, C.C., G.S. and S.F.; Resources, C.C., M.S., A.M. (Alessandro Maturilli), A.S., A.M. (Alessandra Montanini) and J.H.; Data Curation, A.M. (Alessandro Maturilli), C.C. and G.S.; Writing—Original Draft Preparation, C.C.; Writing—Review & Editing, C.C., S.F., M.S., A.S. and A.M. (Alessandra Montanini); Supervision, J.H. Funding Acquisition, G.S. and C.C. All authors have read and agreed to the published version of the manuscript.

Funding

This work was supported by TNA Europlanet 2020 RI, grant No 654208, funded from the European Union’s Horizon 2020 research and innovation programme. CC also want to thank the Italian Space Agency (SIMBIO-SYS project within ASI-INAF agreement 2017-47-H.0).

Data Availability Statement

Data available on request due to restrictions related to DLR database.

Acknowledgments

Authors want to thank two anonymous reviewers and the third, Larry Nittler, that help to improve the manuscript.

Conflicts of Interest

The authors declare no conflicts of interest.

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Minerals 14 00062 g001
Figure 1. Emissivity spectra of the different samples at lower temperature (375 K). Blue and cyan arrows indicate maxima and minima of Mg-GN endmember, respectively; red and orange arrows indicate maxima and minima of CaS, respectively. See text for more details on absorptions.
Figure 1. Emissivity spectra of the different samples at lower temperature (375 K). Blue and cyan arrows indicate maxima and minima of Mg-GN endmember, respectively; red and orange arrows indicate maxima and minima of CaS, respectively. See text for more details on absorptions.
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Minerals 14 00062 g002
Figure 2. Emissivity spectra of the different samples. From top to bottom Mg-GN; 20% CaS; 40% CaS; 60% CaS. Blue and cyan arrows (labeled in Figure 1) on top plot indicate maxima and minima of Mg-GN, respectively; red and orange arrows on bottom plot indicate maxima and minima of CaS, respectively. See text for more details on absorptions.
Figure 2. Emissivity spectra of the different samples. From top to bottom Mg-GN; 20% CaS; 40% CaS; 60% CaS. Blue and cyan arrows (labeled in Figure 1) on top plot indicate maxima and minima of Mg-GN, respectively; red and orange arrows on bottom plot indicate maxima and minima of CaS, respectively. See text for more details on absorptions.
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Figure 3. Variations in the position of the CF plotted against fraction of Mg-GN (top) and temperature (bottom).
Figure 3. Variations in the position of the CF plotted against fraction of Mg-GN (top) and temperature (bottom).
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Figure 4. The positions of the RBs plotted against the fraction of Mg=−GN (left) and temperature (right).
Figure 4. The positions of the RBs plotted against the fraction of Mg=−GN (left) and temperature (right).
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Figure 5. The position of RBs plotted against the fraction of Mg-GN (top) and temperature (bottom), highlighted for RBs 1,2 (a,c) and RBs 3,4 (b,d).
Figure 5. The position of RBs plotted against the fraction of Mg-GN (top) and temperature (bottom), highlighted for RBs 1,2 (a,c) and RBs 3,4 (b,d).
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Figure 6. The spectra plotted against the temperature (top) and the fraction of Mg-GN (bottom).
Figure 6. The spectra plotted against the temperature (top) and the fraction of Mg-GN (bottom).
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Table 1. Position of CF (cm−1) and RBs (cm−1) of emissivity spectra collected at 375 K. Error in position is attributable to spectral resolution, and it is ±2 cm−1.
Table 1. Position of CF (cm−1) and RBs (cm−1) of emissivity spectra collected at 375 K. Error in position is attributable to spectral resolution, and it is ±2 cm−1.
Sample CFRB0RB1RB2RB3RB4RB1*RB4*RB5
Mg-gabbronorite (Mg-GN)122911131001959928876------
20% CaS 1076--1001959924872------
40% CaS 1078--1005959920870------
60% CaS 1097--1009959916868------
CaS 1099----------1038885833
nb: -- means no data.
Table 2. Position of CF (cm−1) and RBs (cm−1) of emissivity spectra collected at 475 K, 575 K and 675 K. Error in position is attributable to spectral resolution, and it is ±2 cm−1.
Table 2. Position of CF (cm−1) and RBs (cm−1) of emissivity spectra collected at 475 K, 575 K and 675 K. Error in position is attributable to spectral resolution, and it is ±2 cm−1.
Sample Temperature (K)CFRB0RB1RB2 RB3 RB4 RB1* RB4* RB5
Mg-gabbronorite (Mg-GN)475123011111003957926876------
575123011071003953924876------
675123011051003951922876------
20% CaS 4751074--1005959926874------
5751074--1005955924874------
6751076--1003953920874------
40% CaS 4751092--1011959920868------
5751090--1009955916868------
6751090--1009955920868------
60% CaS 4751095--1014959914866------
5751094--1014955910862------
6751092--1018957914864------
CaS 4751099----------1038883820
5751097----------1034883794
6751085----------1026881804
nb: -- mean no data.
Table 3. Emissivity values and relative intensity (SC) of CF and RBs of spectra collected at 375 K, 475 K, 575 K and 675 K.
Table 3. Emissivity values and relative intensity (SC) of CF and RBs of spectra collected at 375 K, 475 K, 575 K and 675 K.
SampleTemperature (K)CFRB1RB2 RB3 RB4 RB1* RB4* SCRB1SCRB2SCRB3SCRB4SCRB1*SCRB4*
Mg-gabbronorite (Mg-GN)3750.8950.8030.7890.8000.830----0.0920.1050.0940.065----
4750.8910.7810.7710.7830.813----0.1100.1200.1070.078----
5750.8890.7630.7500.7590.786----0.1260.1390.1300.103----
6750.8930.7630.7530.7610.789----0.1300.1400.1310.104----
20% CaS3750.8750.8050.7970.8050.824----0.0710.0780.0710.051----
4750.8430.7940.7940.8060.827----0.0490.0490.0360.016----
5750.8270.7810.7800.7900.808----0.0460.0460.0370.018----
6750.8150.7640.7620.7700.789----0.0510.0530.0450.026----
40% CaS3750.8870.8210.8170.8230.832----0.0670.0700.0640.055----
4750.8370.7830.7920.8020.809----0.0540.0450.0350.028----
5750.8740.8090.8140.8180.819----0.0650.0600.0570.055----
6750.8500.7900.8010.8080.814----0.0600.0500.0430.037----
60% CaS3750.8940.8140.8170.8220.827----0.0790.0770.0720.067----
4750.8680.7880.8060.8130.813----0.0800.0630.0550.056----
5750.8690.7770.7940.7940.788----0.0910.0750.0740.081----
6750.8220.7510.7760.7830.782----0.0710.0460.0390.040----
CaS3750.975--------0.7340.796--------0.2410.179
4750.974--------0.6850.764--------0.2890.210
5750.965--------0.6580.722--------0.3070.243
6750.978--------0.6580.690--------0.3200.288
nb: -- mean no data.
Table 4. Position of other features attributable to CaS at wavenumber greater than CF. Error in position is attributable to spectral resolution, and it is ±2 cm−1.
Table 4. Position of other features attributable to CaS at wavenumber greater than CF. Error in position is attributable to spectral resolution, and it is ±2 cm−1.
Max B1 (cm−1)Min B1 (cm−1)Max B2 (cm−1)Min B2 (cm−1)Max B3 (cm−1)Min B3 (cm−1)Max B4 (cm−1)Min B4 (cm−1)
20 %CaS37515161508143514271209120011511119
47515141508143114211205119611361115
575150815021431--1203119211261121
675150615021427--1200119411301117
40 %CaS37515161504143713541209120311491121
47515141453143513541203119611361117
57515101493143513561198119411321117
67515081501143113791202119211301115
60 %CaS37515161504143713461207120311481136
47515141497143513421202119811361128
57515101483143513501200119611341124
67515101493143313581200119411321122
CaS37515161499143913541209119611441128
47515141489143713421205119411401124
57515121483143513401202119011361121
67515081481143113481200117811341121
nb: -- mean no data.
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Carli, C.; Ferrari, S.; Maturilli, A.; Serventi, G.; Sgavetti, M.; Secchiari, A.; Montanini, A.; Helbert, J. Laboratory Emissivity Spectra of Sulphide-Bearing Samples, New Constraints for the Surface of Mercury: Oldhamite in Mafic Aggregates. Minerals 2024, 14, 62. https://doi.org/10.3390/min14010062

AMA Style

Carli C, Ferrari S, Maturilli A, Serventi G, Sgavetti M, Secchiari A, Montanini A, Helbert J. Laboratory Emissivity Spectra of Sulphide-Bearing Samples, New Constraints for the Surface of Mercury: Oldhamite in Mafic Aggregates. Minerals. 2024; 14(1):62. https://doi.org/10.3390/min14010062

Chicago/Turabian Style

Carli, Cristian, Sabrina Ferrari, Alessandro Maturilli, Giovanna Serventi, Maria Sgavetti, Arianna Secchiari, Alessandra Montanini, and Jörn Helbert. 2024. "Laboratory Emissivity Spectra of Sulphide-Bearing Samples, New Constraints for the Surface of Mercury: Oldhamite in Mafic Aggregates" Minerals 14, no. 1: 62. https://doi.org/10.3390/min14010062

APA Style

Carli, C., Ferrari, S., Maturilli, A., Serventi, G., Sgavetti, M., Secchiari, A., Montanini, A., & Helbert, J. (2024). Laboratory Emissivity Spectra of Sulphide-Bearing Samples, New Constraints for the Surface of Mercury: Oldhamite in Mafic Aggregates. Minerals, 14(1), 62. https://doi.org/10.3390/min14010062

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