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Article

Insights on Structure and Threshold Detection Limits of Stichtite (Magnesium-Chromium Carbonate-Hydroxide) by Fourier Transform Infrared Analysis

by
Erik Melchiorre
1,2,*,
Andy Garcia
1 and
Maryjo Brounce
2
1
Department of Geological Sciences, California State University of San Bernardino, 5500 University Parkway, San Bernardino, CA 92407, USA
2
Department of Earth and Planetary Sciences, University of California Riverside, 900 University Avenue, Riverside, CA 92521, USA
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(3), 215; https://doi.org/10.3390/min10030215
Submission received: 23 January 2020 / Revised: 23 February 2020 / Accepted: 25 February 2020 / Published: 28 February 2020
(This article belongs to the Section Crystallography and Physical Chemistry of Minerals & Nanominerals)
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Abstract

:
Spectral features for natural stichtite at 1042, 1096, 1360, 1638, and 3482 cm−1 provide insights on mineral structure, with peaks consistent with OH− stretching modes bound to Mg or Cr, CO32− antisymmetric stretches and CO32− bound within the sample and molecular water. These Infrared (IR) data suggest natural stichtite forms at a pH of >12 with increased water and decreased carbonate in the interlayer due to a smaller interlayer distance and unit cell. Higher pH favors lower divalent cation purity and may explain observed ranges of non-end member compositions in stichtite from localities around the world, and across geologic time. This constrains stichtite formation to a range of very high pH conditions and is consistent with active serpentinizing fluid vents and some mine wastes. IR has clear application for the detection and quantification of stichtite under field and laboratory conditions within the detection limits of 5% stichtite within a serpentine host. The size and grade of terrestrial stichtite deposits, and resolution of remote sensing instruments, suggest remote IR detection of stichtite is possible, and remote IR detection for Earth and Mars is discussed.

1. Introduction

Stichtite (Mg6Cr2(OH)16[CO3]·4H2O) is a purple to pink magnesium-chromium hydroxycarbonate mineral that may contain a fossil stable isotope record of early earth serpentinizing conditions under which the Last Universal Common Ancestor (LUCA) is known to have thrived [1,2,3]. Stichtite is an end member of the rhombohedral hydrotalcite group, which includes stichtite (Cr), pyroaurite (Fe), and hydrotalcite (Al). Stichtite has a waxy to pearly luster and has never been reported as macroscopic crystals, but occurs as fine, platy to acicular aggregates of crystallites to crystals typically less than 2 mm in the longest dimension. An excellent review of stichtite is found in Reference [4].
Stichtite is believed to form during active serpentinization, based upon the cross-cutting relations and intergrowth textures [5,6,7]. Serpentinization occurs when water-rock reactions drive the alteration of low-silica ultramafic rocks to form serpentine, hydrotalcite minerals, and other reaction products. This produces an environment with abundant electron donors, such as hydrogen gas and methane, and a high pH, e.g., [8,9]. Stichtite from the south Iberia Abyssal Plain in the Atlantic ocean, just offshore of the Spain-Portugal border, is known to form under these conditions at the expense of brucite and Cr spinel, based upon mineralogical evidence [10], presumably with the reaction MgCr2O4 + 5Mg(OH)2 + CH4 + 2O2 + 5H2O = Mg6Cr2(OH)16[CO3]·4H2O. Similarly, stichtite may form through reaction of hydrogen gas and dissolved inorganic carbon (DIC) [11] with brucite and Cr spinel as MgCr2O4 + 5Mg(OH)2 + CO32− + H2 + 6H2O = Mg6Cr2(OH)16[CO3]·4H2O, given that high pH conditions common to serpentinizing fluids should favor dissolved organic carbon as CO32−.
Understanding the conditions that occur during active, modern serpentinization has greatly increased our knowledge of these systems and their role in supporting microbial life and the generation of methane, e.g., [12,13]. This, in turn, informs our understanding of possible sources of methane on modern and ancient Mars, and its implications for biosignatures, e.g., [9,14,15]. Geochemical results from recent work on active serpentinizing systems [10,11] suggest conditions similar to those indicated by work on stichtite from Archean and Phanerozoic serpentinites [2,3].
Hydrotalcite minerals such as stichtite are known to store molecules such as peptides and amino acids within the hydrated interlayer between their brucite-like layers, e.g., [16,17,18,19]. As a carbonate, stichtite is likely to be among the most suitable of the serpentinization products for capture and preservation of direct-proxy carbon cycle biosignatures. However, questions remain about secondary formation of hydrotalcite minerals, and the potential environmental exchange of the loosely-bound contents of the interlayer, while the possibility of isotopic exchange for the contents of other more structurally bound signals in other portions of the stichtite structure remains unexplored [20,21].
If stichtite within serpentinite from fossil hydrothermal systems does preserve an isotope record of its conditions of formation, and harbor organic molecules in its interlayer, it would provide a window into conditions of habitable environments on early earth. As serpentinite is believed to occur in rocks from early Mars, e.g., [22,23] when water and an atmosphere were likely present, e.g., [24], it is possible that stitchtite may also be present, particularly in those rocks which were likely formed in the subsurface in closed systems and elevated temperatures, e.g., [25]. Here, we present infrared spectra of stitichtite and serpentine from the minerals’ type locality at Stichtite Hill, Tasmania, Australia, in order to assess the extent to which trace stitchtite can be observed spectroscopically. While the mere presence of stichtite or other hydrotalcite minerals is not itself a biomarker, the ability to detect it remotely (e.g., through orbiter-mounted infrared spectroscopy) would mark an attractive target in the search for a record of life on early Earth and Mars. Thus it is important to determine the structural properties of stichtite which may harbor or preserve biomarkers, and determine the threshold at which remote sensing instrumentation like the Compact Reconnaissance Imaging Spectrometer for Mars (CRISM), and direct-contact instrumentation like Fourier transform infrared (FTIR), can distinguish the presence of stichtite in serpentinite.

Geology and Mineralogy of Samples Used in this Study

The stichtite occurrences of Tasmania, Australia are hosted by serpentinized mid-Cambrian ultramafic rocks known as the Dundas ultramafic complex [26,27]. This unit consists of heavily serpentinized ultramafic rocks, gabbros, and basaltic volcanic rocks. Three types of serpentinite are recognized in these rocks [28]. There are black serpentinites—these are unsheared, often contain abundant fine-grained magnetite, and are dominantly lizardite, which has replaced olivine-bearing ultramafic rocks. There are also green serpentinites, which are lizardite-chrysotile mixtures with localized deformation patterns and brecciation. Finally, there are sheared-contact serpentinites that consist mainly of chrysotile and rare antigorite, and may have formed during tectonic emplacement of the Adamsfield Ultramafic Complex [29]. All three of these serpentinite bodies lie within Middle to Late Cambrian strata. Stichtite mineralization occurs mainly within massive chromite-rich green serpentinite, and rarely within its border zones with black serpentinite [30]. Stichtite has a strong association with zones of brecciated green serpentinite [30].
Samples for this study come from the Stichtite Hill locality of Tasmania, Australia, which is the type location for this mineral species. Stichtite was first noted at this locality in 1891 [31], though it was another 23 years before it was properly described as a new species, because of miss-identification of the mineral [32]. All samples were collected by the authors from freshly mined material.

2. Materials and Methods

2.1. Sample Preparation and Characterization

Whole-rock samples of green serpentinite with purple stichtite were collected from the Stichtite Hill locality described above (Figure 1 and Figure 2). These samples were specifically selected from a location at the mine where the deepest excavations had exposed fresh material. Sample billets were cut from these rocks to expose fresh material just prior to sample preparation and analysis. Samples were selected to include a wide range of proportions of stichtite and serpentine minerals. Samples for scanning electron microscope energy dispersive analyses (SEM/EDX) and FTIR analyses were cut with a rock saw into 1–3 cm billets, ground flat, and polished to 0.2 μm with alumina grit. Samples for x-ray diffraction (XRD) analyses were broken off the larger billets described above. These chips were coarsely crushed and hand-picked to produce separate stichtite and serpentine concentrates which were then crushed to <0.25 mm. The concentrate was then processed with a Frantz vibro-magnetic separator to remove chromite and other impurities, then crushed to pass through a 100-mesh screen (<0.147 mm). Resulting powders were scanned by x-ray diffraction (XRD) to confirm mineralogy.

2.2. Geochemical Analyses

The XRD analyses were performed on a Philips X-Pert diffractometer (Philips Electronic Instruments, Inc., Mahwah, NJ, USA). A Philips Electronics Instruments Silicon Powder Standard (Type N: 52131) and an alpha quartz sample from Hot Springs, Arkansas were run as XRD standards. Centroid peak errors on the standards were ±0.002 2θ. In addition to XRD analyses, SEM/EDX was used to examine all polished samples to confirm mineralogy by chemistry and stoichiometry. A Phenom XL SEM (Fisher Scientific, Phoenix, AZ, USA) was used to capture secondary electron (SE) and backscatter electron (BSE) images using an acceleration voltage of 2 or 15 kV, respectively. The same instrument was used for energy dispersive X-ray (EDX) element measurements of major and minor element abundances, using standard off-peak interference and matrix corrections [33,34,35,36,37,38], and calibrations with registered standards provided by the manufacturer. The error associated with the in-situ element analyses is less than ±2%. Additional details on SE/BSE imaging and chemistry of samples from this locality are found in [2,7].
The geochemical characterization of stichtite from the Stichtite Hill locality has been previously performed by many authors, e.g., [30,36,37] and is summarized in graphical and tabular form in Figure 5 and Table 2 in Reference [2]. Mineralogically, these correspond to a range of compositions from near endmember stichtite to iron- and aluminum-rich stichtite. Additionally, the crystal structure has been significantly refined within the hydrotalcite group, and the related species Barbertonite was discredited and recognized as Stichtite-2H by [35,38].

2.3. FTIR Analyses

Singly polished billets were analyzed via total reflectance Fourier transform infrared spectroscopy (FTIR) on a Thermo-Nicolet iS50 bench with Continuum Microscope attachment and a hemispherical silicon ATR crystal. The silicon crystal makes contact with the sample in 120 μm diameter patches, and the incident beam samples ~0.6 μm depth at 2000 cm−1. Spectra were collected in nominally dry, CO2-free air produced from a Parker-Ballston purge-gas generator at ~30 scfh, from 650 to 6000 cm−1 on a liquid nitrogen cooled MCT-A detector. Background spectra were collected in dry, CO2-free air (i.e., with no sample contact) and were subtracted from sample spectra shown in Figure 3, Figure 4, Figure 5 and Figure 6.

3. Results

Three sets of stichtite-serpentine mineral separates from the Stichtite Hill locality were examined by XRD. All samples were confirmed as either stichtite or a mixture of serpentine minerals (~90% lizardite, ~10% chrysotile) by XRD analysis. Examination of polished billets by SEM/EDX yielded major element chemistry and stoichiometry consistent with the presence of stichtite and serpentine mineralogy. In most samples, highly reflective domains of chromite within stichtite, and magnetite within serpentinite, were identified (Figure 2).
The results of FTIR analyses of unoriented stichtite and serpentine (i.e., lizardite +/− chrysotile) are presented in Figure 3, Figure 4, Figure 5 and Figure 6. Stichtite shows prominent and generally broad spectral features at 1042, 1096, 1360, 1638, and 3482 cm−1. The serpentine matrix shows prominent and generally narrow, intense spectral features at 938 and 3680 cm−1 (Figure 3). The group of peaks from 3680 cm−1 to 3482 cm−1 correspond to the position of peaks that arise from OH− stretching modes, where OH− groups are bound to Mg (serpentine and stitchtite) or Cr (stitchtite). An intense peak due to CO32− antisymmetric stretches appears in stichtite at 1360 cm−1, which is absent in serpentine. This is ~20 cm−1 lower than the previous measurements of synthetic stichtite (e.g., this peak is reported to appear at 1381 cm−1 by [39]), suggesting either (1) a compositional dependence on the cation identity bound to the carbonate anionic group and/or (2) an analytical dependence on the composition of the ATR crystal (diamond ATR in [39] versus a silicon ATR in this study). There are smaller doublets that appear. It is possible that these arise because of insufficient “background” subtraction, i.e., there is CO2 from atmosphere gases in the path of the IR beam that are not fully accounted for during the analysis. The doublet peaks at 1096 and 1042 cm−1 may be interpreted either as CO32− bound in the stichtite, or potentially is interference from nearby serpentine that is inadvertently included in the analytical volume. Because the analytical volume is relatively small relative to the size of some stichtite pods, we prefer the former interpretation. The stichtite spectra also shows a dominant peak at 1638 cm−1, which is a deformation mode of molecular water, and is not present in the measurements of the serpentine matrix. The serpentine matrix has a sharp, intense peak at 938 cm−1 with an apparent, lower intensity shoulder at higher wave numbers. This peak is absent in stitchtite analyses and is attributed to Si–O bond motions in the silica tetrahedron in lizardite +/− chrysotile.
Measurements of regions in samples at the boundary between stichtite pods and serpentine matrix, contain all of the characteristic spectral features of stichtite, but also contain a peak at 938 cm−1, which is attributed to Si–O bond stretches (e.g., 2P-4, 2P-9, 1P-2, 6NP-8; Figure 6). The intensity of the peak at 938 cm−1 varies, and the narrow peak at 3680 cm−1 observed in the serpentine matrix is not present in these mixed measurements (Figure 6). This suggests that these analyses contain a silicate mineral in the analysis volume, but that it lacks the highly ordered Mg–OH stretches observed in the lizardite +/− chrysotile serpentine matrix (Figure 3 and Figure 4). One possibility is that these analyses contain traces of clinochore in addition to stichtite. Clinochore is known to be present in stichtite pods from the more altered samples from the same mine (Figure 3b in Reference [7]), present as veinlets that pervade and surround the stichtite matrix. Although the samples in this study were selected for freshness, the FTIR spectra suggest that perhaps incipient clinochore veins exist at the boundary between the serpentine matrix and stichtite pods (e.g., 2P-4, 2P-9, 1P-2, 6NP-8) and also within some stichtite pods (6NP-6, 2P-5, and 2P-2).
The key observation in this study is that the spectral features of the serpentine matrix and stichtite pods are distinct in both wavenumber position and spectral forms as the result of the variety of incorporation mechanisms for H, C, and Si in each mineral, and can be readily distinguished from one another with stichtite being prominent at concentrations as low as 5%.

4. Discussion

4.1. Structural and Geochemical Insights

The stichtite spectral features at 1042, 1096, 1360, 1638, and 3482 cm−1 provide multiple insights on the structure of this mineral. The group of peaks at 3482 cm−1 is consistent with the peaks that arise from OH− stretching modes, where OH− groups would be bound to Mg or Cr. The intense peak at 1360 cm−1 is consistent with CO32− antisymmetric stretches. The smaller doublets that appear in stichtite spectra at 1096 and 1042 cm−1 are interpreted as CO32− bound within the sample. The stichtite spectra also shows a dominant peak at 1638 cm−1 which is a deformation mode of molecular water. This is consistent with what is known about the structure of stichtite from other studies [4,39].
In addition to structural insights, the IR data provide suggestions on the chemical conditions under which stichtite may have formed. Experimental work by [36] has linked Cr-Zn hydrotalcite (Mg6Al2(CO3)(OH)16·4H2O) formation at increasing pH to increased water and decreased carbonate in the interlayer. This decrease in carbonate leads to decreased repulsive charges and decreased interlayer distance and unit cell.
Comparison of our IR data (Figure 4) with the experimental IR data in Figure 3 from [36] suggests that the Stichtite Hill samples formed at a pH of at least 12. While it is no surprise that stichtite would form at very high pH, given the known formation under serpentinizing conditions, e.g., [2,10,41,42], this does provide important supporting evidence for the conditions under which stichtite may form. It also suggests that the increased water and decreased carbonate in the interlayer associated with very high pH formation produces a smaller interlayer distance and unit cell for the samples we studied.
It has been puzzling for early researchers why stichtite occurs in only a few chromite-rich serpentinites, if it is indeed only a surface weathering product. It is now reported that stichtite and other hydrotalcite minerals will form as a surface weathering product when ultramafic mine tailing pore water has pH 8.4 to 9.1 [38] and 8.8 to 9.4 [43]. It is also known that stichtite can form in active deep-sea submarine serpentinizing systems with pH 9 to 12.5 conditions [10,11,44,45]. Based on these observations, and the similarity of stichtite IR data for Stichtite Hill and synthetic hydrotalcite grown at >12 pH, it seems most likely that stichtite formation is restricted to chromite-rich bodies with extremely high pH. Furthermore, the inferred >12 pH conditions under which stichtite from Stichtite Hill is believed to have formed is most consistent with formation conditions found in active hydrothermal serpentinizing systems, and not the generally lower pH conditions found in most ultramafic mine tailing pore waters. This does not preclude formation of stichtite from weathering mine tailings, but serves as a tool by which it may be possible to determine the mode of formation from the rock record.
Additional work by [40] used a combination of synthesis experiments and IR analyses to determine that lower pH conditions favor higher divalent cation purity, while higher pH favors formation of metal oxides. This observation is significant for several reasons. First, it may explain the observed range of non-end member compositions observed in stichtite from localities around the world, and across geologic time [2,3]. While it is possible that these compositional trends may reflect the abundance of reactants within the serpentinizing system, it is also possible that this compositional variation is a record of serpentinizing fluid pH. In host material with high porosity and permeability, such as ultramafic mine tailings, it has been demonstrated that stichtite can form as a weathering product, and exchange ions with the pore waters [42,43]. Future workers should explore the possibility of mapping spatially this potential fossil pH record for specific deposits, and examine the ion exchange capacity of this mineral, and specifically which sites may be prone to exchange, and which may bind ions more tightly.
Second, the “oxidation-reduction paradox” of formation of magnetite during serpentinization conditions of low oxygen fugacity and high partial pressures of hydrogen) [13] has been explained as a phenomena of grain boundary fluid buffering. Work by [40] determined experimentally and with FTIR studies that higher pH favors formation of metal oxides in competition with hydrotalcite, presenting a viable mechanism for the formation of the magnetite which is commonly found in close association with stichtite in serpentinite bodies. It is possible that the grain boundary buffering is mediated to some extent by the pH effects of metal oxide-hydrotalcite competition. The work of [41] established that serpentinite with abundant magnetite and Fe-poor brucite formed at temperatures of 200–300 °C, while magnetite-poor samples with Fe-rich brucite formed at temperatures <200 °C. By analog to the above work and experimental FTIR studies, it is possible that thermal profiles of stichtite-rich serpentinizing vents may be generated by a combination of mapping Fe-substitution in stichtite and magnetite abundance at specific sites. Special focus on localities where stichtite and stichtite-2H (nee: Barbertonite) both occur such as Nevada Creek, Tasmania, Australia, and Barberton, South Africa may prove exceptionally rewarding as the 2H polytype of other hydrotalcite minerals is believed to form at higher temperatures [46].

4.2. Determination of FTIR Detection Threshold for Stichtite in Serpentine and Implications for Astrobiology

If stichtite preserves a faithful isotopic record of the conditions in which it formed during the Archean to Neo-Cambrian, and given the modern association of this type of environment with primitive chemosynthetic Archea, it is an exciting possibility that stichtite may record biosignatures from early earth, e.g., [3]. As serpentinizing environments are known to exist on Mars, it is further possible that hydrotalcite minerals such as stichtite may preserve past or present biosignatures within Martian serpentinite terrains.
The determination that stichtite formation is associated with potentially habitable environments, and may record these conditions and their carbon sourcing as far back as the Archean will have utility for interpretation of potential biosignatures on Mars. The possibility that stichtite may also preserve an isotopic and geochemical record from both deep-Earth time in tightly-bound structural sites, and a more recent signal from a loosely-bound interlayer that is more readily exchanged, could provide a powerful time-vector for biological change [21].
The requirements for serpentinization are simply heat, water, and mafic rock. Serpentinite is known to occur in rocks from early Mars, e.g., [22,23], when water, heat flow, and an atmosphere were likely present over large mafic bedrock terrains, e.g., [24]. Serpentinization would have generated H2 and methane which are known energy sources for the earliest chemosythetic life on earth [1]. A record of these habitable environments on Mars may be preserved within stichtite or other hydrotalcite minerals in these serpentinite rocks. The association of modern excess methane with these same terrains should be used to supplement existing evidence for site selection of future Mars sample cache/return missions, as well as instrumentation choice [47], as the best analog between Earth and Mars may be found by viewing the past and present habitable environmental conditions through the lens of deep-earth time during terrestrial serpentinization, when known biological systems were more primitive, e.g., [48].
The use of IR has clear application for the detection and quantification of minor amounts of stichtite under field and laboratory conditions. At both the hand-sample scale (Figure 2) and outcrop scale (Figure 7), stichtite abundance is typically well above 5% of the serpentine host for the brecciated pipes within which it occurs. At the Stichtite Hill, Tunnel Hill, and Nevada Creek localities in Tasmania, Australia, stichtite is observed to locally comprise over 50% of the rock at the scale of 0.1 to 1 m (Figure 7), with a footprint of up to 100 m for abundances at the 5% cutoff. Assuming that stichtite deposit formation would be similar on Mars, and given the resolution of existing instrumentation, this suggests that IR spectra from both remote sensing and lander/rover missions will have the potential to detect stichtite within serpentinite terrains.
If stichtite records biosignatures and formation conditions from early earth it may also record conditions of formation in serpentinizing environments that are known to exist on Mars. The use of IR has clear application for the detection and quantification of minor amounts of stichtite under field and laboratory conditions. At both the hand-sample scale and outcrop scale, stichtite abundance is typically well above the IR detection limits of 5% of the serpentine host. With a typical stichtite deposit footprint of up to 10,000 m2 for abundances at the 5% cutoff, and given the resolution of existing instrumentation, this suggests that IR spectra from both remote sensing and lander/rover missions will have the potential to detect stichtite within the serpentinite terrains on Mars.

5. Conclusions

Stichtite spectral features at 1042, 1096, 1360, 1638, and 3482 cm−1 provide insights on mineral structure. Peaks at 3482 cm−1 are consistent with OH− stretching modes, where OH− groups would be bound to Mg or Cr. The 1360 cm−1 peak is consistent with CO32− antisymmetric stretches, and smaller doublets at 1096 and 1042 cm−1 are interpreted as CO32− bound within the sample. The dominant stichtite peak at 1638 cm−1 is a deformation mode of molecular water.
In addition to structural insights, the IR data suggests constraints on the chemical conditions under which stichtite may have formed, as experimental work has linked increasing pH to increased water and decreased carbonate in the interlayer of hydrotalcite. This decrease in carbonate leads to decreased repulsive charges and decreased interlayer distance and unit cell. Comparison of our IR data with IR data from [40] suggests that natural stichtite formed at a pH of >12. While it is no surprise that stichtite would form at very high pH, given the known formation under serpentinizing conditions, this does provide important evidence for conditions of stichtite formation. It also suggests that the increased water and decreased carbonate in the interlayer associated with very high pH formation produces a smaller interlayer distance and unit cell for the samples we studied.
Additional work by [40] determined that lower pH conditions favor higher divalent cation purity, while higher pH favors formation of metal oxides. This observation may explain the observed range of non-end member compositions observed in stichtite from localities around the world, and across geologic time. While it is possible that these compositional trends may reflect the abundance of reactants within the serpentinizing system, it is also possible that this compositional variation is a record of serpentinizing fluid pH. If so, the wide compositional trends seen in stichtite from Tasmania and Mt. Keith Australia, Mexico, and South Africa may link stichtite formation to a range of very low pH conditions.
It is puzzling why stichtite occurs in few of the many chromite-rich serpentinites, if it is indeed only a surface weathering product. Stichtite and other hydrotalcite minerals will form as a surface weathering product when pore water pH is elevated, but it is also known that stichtite can form in active deep-sea serpentinizing systems with elevated pH. Based on these observations, the wide-ranging composition of stichtite, and the similarity of stichtite IR data for Stichtite Hill and synthetic hydrotalcite grown at >12 pH, it seems most likely that stichtite formation is restricted to chromite-rich bodies with extremely high pH. This is most consistent with formation conditions found in active hydrothermal serpentinizing systems, and less commonly the generally lower pH conditions found in most ultramafic mine tailing pore waters. This does not preclude formation of stichtite from weathering mine tailings.

Author Contributions

Conceptualization and methodology, E.M. and M.B.; analysis and field work, E.M. and A.G.; funding acquisition and instrumentation support, M.B. and E.M.; writing—original draft preparation, review and editing, visualization, E.M., M.B., and A.G.; supervision and project administration, M.B. and E.M. All authors have read and agreed to the published version of the manuscript.

Funding

Instrumentation was provided and supported by the National Science Foundation, EAR-0115884 and EAR-0941106 (E.M.) and the University of California (M.B.). Support of SEM, EDX, and XRD instrumentation was by a California State University VETI grant (E.M., Tim Usher, and Codi Lazar). Support was provided by a NASA Astrobiology Institute Minority Institution Research Sabbatical (NAI-MIRS) program award to one of the authors (E.M.), and his student (A.G.).

Acknowledgments

We thank Mike and Eleanor Phelan for providing access to their mining properties, being generous hosts, and providing valuable insights on stichtite occurrence gained from decades of experience on mining stichtite for collectors and ornamental use. We also thank Ralph Bottrill (Mineral Resources Tasmania), Sue Koepke, and Geert Buters (both Mineralogical Society of WA) for support in the field and valuable discussions on the occurrence and origins of stichtite. Students Kahn Luu, Samantha Harris, and Zach Freeman assisted with fieldwork and lab work as a senior project at CSUSB. The lead author also thanks his colleagues in the Minority Institution Astrobiology Collaborative (MiAC), and the astrobiology teams at UC Riverside and University of Hawaii for providing a supportive network and environment which made this work possible.

Conflicts of Interest

The authors declare no conflict of interest. The funders had no role in the design of the study; in the collection, analyses, or interpretation of data; in the writing of the manuscript, or in the decision to publish the results.

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Figure 1. Sample location map, showing the location of Stichtite Hill and the Dundas Mining District, Tasmania, Australia (Black Square).
Figure 1. Sample location map, showing the location of Stichtite Hill and the Dundas Mining District, Tasmania, Australia (Black Square).
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Figure 2. Large representative polished billet of serpentine-hosted stichtite. Slight variations in the shade of green for the serpentine result from slight variations (±4%) in the ratio of lizardite to chrysotile. Black veinlets within the green serpentine are magnetite. The purple stichtite domains contain silvery-black fragments of chromite.
Figure 2. Large representative polished billet of serpentine-hosted stichtite. Slight variations in the shade of green for the serpentine result from slight variations (±4%) in the ratio of lizardite to chrysotile. Black veinlets within the green serpentine are magnetite. The purple stichtite domains contain silvery-black fragments of chromite.
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Figure 3. Plot of Fourier transform infrared spectroscopy (FTIR) spectra of stichtite (purple line) and its serpentine (lizardite) mineral host (green line). The peak positions in wavenumbers (cm−1) for stichtite key features are marked with dashed vertical lines. Peak positions in wavenumbers (cm−1) for key features in serpentine are marked with vertical solid lines. Peaks between 3700 and 3482 cm−1 correspond to OH− stretching modes. The 1638 cm−1 peak is a deformation mode of molecular H2O. The 1360 cm−1 peak is a CO32− antisymmetric stretching mode. The 938 cm−1 peak corresponds to Si–O vibrations in the SiO42− tetrahedron.
Figure 3. Plot of Fourier transform infrared spectroscopy (FTIR) spectra of stichtite (purple line) and its serpentine (lizardite) mineral host (green line). The peak positions in wavenumbers (cm−1) for stichtite key features are marked with dashed vertical lines. Peak positions in wavenumbers (cm−1) for key features in serpentine are marked with vertical solid lines. Peaks between 3700 and 3482 cm−1 correspond to OH− stretching modes. The 1638 cm−1 peak is a deformation mode of molecular H2O. The 1360 cm−1 peak is a CO32− antisymmetric stretching mode. The 938 cm−1 peak corresponds to Si–O vibrations in the SiO42− tetrahedron.
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Figure 4. FTIR spectra for serpentine matrix in samples 6NP and 1P.
Figure 4. FTIR spectra for serpentine matrix in samples 6NP and 1P.
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Figure 5. FTIR spectra for stichtite nodules in samples 2P, 6NP, 4P. Red spectra is a synthetic stichtite precipitated from fluids with pH > 12 [40].
Figure 5. FTIR spectra for stichtite nodules in samples 2P, 6NP, 4P. Red spectra is a synthetic stichtite precipitated from fluids with pH > 12 [40].
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Figure 6. FTIR spectra from the boundary between stitchtite nodules and the serpentine-host, deliberately including both stitchtite and serpentine in the analyses volume, in samples 2P, 6NP, and 1P (black lines). Also shown are the FTIR spectra of stichtite (purple line, top) and serpentine host (green line, bottom) from Figure 3.
Figure 6. FTIR spectra from the boundary between stitchtite nodules and the serpentine-host, deliberately including both stitchtite and serpentine in the analyses volume, in samples 2P, 6NP, and 1P (black lines). Also shown are the FTIR spectra of stichtite (purple line, top) and serpentine host (green line, bottom) from Figure 3.
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Figure 7. Outcrop-scale photograph of stichtite occurrence and abundance at Stichtite Hill, Tasmania, Australia. Stichtite (purple areas) constitute about 50% of this outcrop, with the balance being serpentine (shades of green) and pyroaurite (brownish-red). Geologist is 1.6 m tall.
Figure 7. Outcrop-scale photograph of stichtite occurrence and abundance at Stichtite Hill, Tasmania, Australia. Stichtite (purple areas) constitute about 50% of this outcrop, with the balance being serpentine (shades of green) and pyroaurite (brownish-red). Geologist is 1.6 m tall.
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Melchiorre, E.; Garcia, A.; Brounce, M. Insights on Structure and Threshold Detection Limits of Stichtite (Magnesium-Chromium Carbonate-Hydroxide) by Fourier Transform Infrared Analysis. Minerals 2020, 10, 215. https://doi.org/10.3390/min10030215

AMA Style

Melchiorre E, Garcia A, Brounce M. Insights on Structure and Threshold Detection Limits of Stichtite (Magnesium-Chromium Carbonate-Hydroxide) by Fourier Transform Infrared Analysis. Minerals. 2020; 10(3):215. https://doi.org/10.3390/min10030215

Chicago/Turabian Style

Melchiorre, Erik, Andy Garcia, and Maryjo Brounce. 2020. "Insights on Structure and Threshold Detection Limits of Stichtite (Magnesium-Chromium Carbonate-Hydroxide) by Fourier Transform Infrared Analysis" Minerals 10, no. 3: 215. https://doi.org/10.3390/min10030215

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