Ancient Mars had surface liquid water and a dense carbon dioxide (CO2)-rich atmosphere. Such an atmosphere would interact with crustal rocks, potentially leaving a mineralogical record of its presence. We analyzed the composition of an 89-meter stratigraphic section of Gale crater, Mars, using data collected by the Curiosity rover. An iron carbonate mineral, siderite, occurs in abundances of 4.8 to 10.5 weight %, colocated with highly water-soluble salts. We infer that the siderite formed in water-limited conditions, driven by water-rock reactions and evaporation. Comparison with orbital data indicates that similar strata (deposited globally) sequestered the equivalent of 2.6 to 36 millibar of atmospheric CO2. The presence of iron oxyhydroxides in these deposits indicates that a partially closed carbon cycle on ancient Mars returned some previously sequestered CO2 to the atmosphere.

A new glycolate mineral species, rasmussenite, ideally Ca(C2H3O3)2·3H2O, was discovered from the western end of Pusch Ridge in the Santa Catalina Mountains, north of Tucson, Arizona, USA. It occurs as sprays or spherical aggregates of fibrous/acicular crystals, with individual crystals up to 0.30 × 0.01 × 0.01 mm. Associated minerals include chrysocolla, hematite, lazaraskeite, microcline, phlogopite, quartz, and stanevansite. Rasmussenite is colorless to white, transparent with a white streak and vitreous luster. It is brittle and has a Mohs hardness of ∼1. No cleavage is observed. The fracture is splintery. The measured and calculated densities are 1.53(5) and 1.55 g/cm3, respectively. Optically, rasmussenite is biaxial (+), with α = 1.446(2), β = 1.472(2), γ = 1.508(2), and 2Vcal. = 63°. The chemical composition was determined by means of both electron microprobe analysis and an elemental combustion system equipped with a mass spectrometer, yielding an empirical formula Ca0.98(C2.00H3.00O3)2·3H1.97O, on the basis of 9 O apfu. Rasmussenite is triclinic with space group P, and unit-cell parameters based on single-crystal X-ray diffraction a = 9.6662(15), b = 9.722(2), c = 5.7628(3) Å, α = 89.959(11), β = 76.761(9), γ = 97.245(15)°, V = 522.71(14) Å3, and Z = 2. It is the natural glycolate counterpart of Ca-glycinate trihydrate, Ca(C2H4NO2)2·3H2O, which was identified recently from human kidney stones. In the rasmussenite structure, each Ca cation is coordinated by four O and four Ow atoms (Ow = O atom in H2O). The four O atoms are associated with two bidentately bonded glycolate anions. The [Ca(O4Ow4)]-polyhedra share Ow–Ow edges to form zigzag chains extending along the c-axis. These chains are interconnected by hydrogen bonds through the uncoordinated Ow3 water molecule. The discovery of rasmussenite, together with other glycolate minerals documented thus far, implies the likelihood of future discoveries of glycinate minerals.

A new organic mineral species, lianbinite, ideally (NH4)(C2H3O3)(C2H4O3), was discovered from the western end of Pusch Ridge in the Santa Catalina Mountains, north of Tucson, Arizona, U.S.A. It occurs as bladed or acicular crystals, associated with baryte, fluorite, glecklerite, jarosite, jimkrieghite, quartz, and rasmussenite. Lianbinite is colorless, transparent with a white streak and vitreous luster. It is brittle and has a Mohs hardness of 1-1 1/2; cleavage is perfect on {100}. No parting or twinning was observed. The calculated density is 1.497 g/cm3. The chemical composition of lianbinite was determined with a Thermo Finnigan DELT Aplus XL Elemental Combustion System equipped with a mass spectrometer, yielding an empirical formula (N0.98H4.06)(C1.98H3O3)(C1.99H3O3), or N0.98C3.97H11.06O6, on the basis of 6 O apfu.Lianbinite is the natural counterpart of synthetic (NH4)(C2H3O3)(C2H4O3), which is isostructural with synthetic K(C2H3O3)(C2H4O3) and Rb(C2H3O3)(C2H4O3). It is monoclinic with space group P21/c, and unit-cell parameters a = 3.91305(11), b = 18.7499(4), c = 10.7214(2) & Aring;, beta = 107.444(2)degrees, V = 750.45(3) & Aring;3, and Z = 4. The crystal structure of lianbinite contains two forms of glycolate units: glycolate anions (GAs) and glycolic acid molecules (GMs). These two units are linked together by hydrogen bonds to form a three-dimensional network with two kinds of channels extending along [100]. The large channel is surrounded by O atoms, with (NH4)+ groups situated inside, whereas the small one is enclosed by H atoms. The discovery of lianbinite, together with eight other glycolate minerals documented thus far, implies that glycolate minerals may be rather widespread in nature, thus serving as a potential reservoir for biologically fixed carbon.

Minerals incorporate 72 different essential elements, many of which are redox sensitive. We compiled oxidation states of ions in 4834 IMA-approved mineral species with oxygen and/or halogens as anions and have identified 87 essential mineral-forming ions. We compiled data on the coexistence of these ions as recorded in their minerals' chemical formulas, and applied methods of network analysis with community detection and heatmap analysis with agglomerative clustering to reveal patterns of ion coexistence.Unipartite networks illustrate the most common coexisting ion pairs, whereas Louvain and Walktrap methods reveal distinct ion groups-patterns that both reinforce and refine the Goldschmidt geochemical classification of elements. Key findings include: (1) that mineral-forming ions group into two major communities with a number of subcommunities; (2) that different ion communities primarily reflect contrasting geochemical and paragenetic processes such as primary igneous mineralisation, hydrothermal precipitation, and near-surface oxidation and weathering, rather than crystal chemical constraints; and (3) that different oxidation states of some redox-sensitive elements fall into two or more of these communities, underscoring how ions of the same elements commonly display contrasting geochemical and/or paragenetic affinities.Heatmap analysis reveals groupings of co-occurring ions that mimic many aspects of community detection methods, as well as significant patterns of ion antipathies-groups of ions that are seldom if ever paired. For example, alkali metals commonly associated with late-stage igneous fluids (Cs+, Li+ and Rb+) rarely co-occur with low field strength ions found concentrated in brines (Ag+, Br-, Cu+, Hg+ and I-) or high field strength ions from weathered primary oxide or sulfide deposits (Cr6+, Pb4+, Mo4+, Te4+ and Te6+). Such ion pairs are well known in synthetic oxides. Therefore, with the exceptions of cations having very different redox potentials, unobserved ion pairs are principally the consequences of element rarity coupled with natural geochemical and paragenetic antipathies rather than crystal chemical constraints.

A new oxalate mineral species, edwindavisite, ideally Cu(C2O4)(NH3), was discovered in specimens collected from the Rowley mine, Maricopa County, Arizona, USA. It occurs as fans or sprays of bladed or prismatic crystals (up to 0.50 x 0.08 x 0.06 mm), associated intimately with ammineite, a sampleite-like mineral, baryte, ebnerite, wulfenite and quartz. Edwindavisite is green, transparent with a pale green streak and has a vitreous lustre. It is brittle and has a Mohs hardness of similar to 2; cleavage is perfect on {100}. No parting or twinning was observed. The measured and calculated densities are 2.55(2) and 2.53 g/cm3, respectively. Optically, edwindavisite is biaxial (+), with alpha = 1.550(2), beta = 1.559(2), gamma = 1.755(5), 2Vmeas. = 26(2)degrees and 2Vcal. = 26.4 degrees. Electron microprobe analyses yielded the empirical formula (based on Cu = 1 apfu) Cu1.00(C2O4)(NH3)0.99.Edwindavisite is the natural counterpart of synthetic catena-mu-oxalato-ammine-copper(II), Cu(C2O4)(NH3). It is orthorhombic with space group Pbca and unit-cell parameters a = 11.1998(10), b = 9.4307(9), c = 8.3977(7) & Aring;, V = 886.98(14) & Aring;3 and Z = 8. In the edwindavisite structure, each Cu2+ cation is coordinated by (5O + N), forming a rather distorted and elongated octahedron. The Cu-octahedra share corners with one another to form chains extending along [001], which are joined together by oxalate (C2O4)2- groups, giving rise to layers parallel to (100). These layers are linked together by N-HO hydrogen bonds. Among 37 oxalate minerals documented to date, edwindavisite is the first one that contains ammonia (NH3).

This study presents mineral composition estimates of rock and sediment samples analyzed with the CheMin X-ray diffraction instrument on board the NASA Mars Science Laboratory rover, Curiosity, in Gale crater, Mars. Mineral composition is estimated using crystal-chemically derived algorithms applied to X-ray diffraction data, specifically unit-cell parameters. The mineral groups characterized include those found in major abundance by the CheMin instrument (i.e., feldspar, olivine, pyroxene, and spinel oxide). In addition to estimating the composition of the major mineral phases observed in Gale crater, we place their compositions in a stratigraphic context and provide a comparison to that of martian meteorites. This work provides expanded insights into the mineralogy and chemistry of the martian surface.

AbstractUnderstanding changes in material properties through external stimuli plays a key role in validating the expected performance of materials and engineering material properties in a controlled manner. Here, we introduce a fundamental protocol to deduce dehydration reactions kinetics of water confined in nanopore channels, with the cyclosilicate beryl as the scaffold of interest, using time-resolved synchrotron X-ray diffraction (SXRD), in the temperature interval of 298–1038 K. The temperature-dependent intensity $$(I)$$ ( I ) of the strongest reflection (112) was used as the crystallite variable. An estimation of an isobaric thermal crystallite coefficient, $$k$$ k , analogous with the isobaric thermal expansion coefficient, established the rate of relative crystallization as a function of temperature, $$\frac{\partial I}{\partial T}$$ ∂ I ∂ T . A plot of $$lnk$$ lnk and $$\frac{1}{T}$$ 1 T gives rise to two kinetic steps, indicating a slow dehydration stage up to ~ 700 K and a fast dehydration stage up to the investigated temperature 1038 K. The crystal structure of beryl determined up to 1038 K, in temperature increment as small as 10 K, indicates the presence of channel ions Na and Fe and a gradual decrease of water upon heating.

For more than a decade, the CheMin X-ray diffraction instrument on the Mars Science Laboratory rover, Curiosity, has been returning definitive and quantitative mineralogical and mineral–chemistry data from ~3.5-billion-year-old (Ga) sediments in Gale crater, Mars. To date, 40 drilled rock samples and three scooped soil samples have been analyzed during the rover’s 30+ km transit. These samples document the mineralogy of over 800 m of flat-lying fluvial, lacustrine, and aeolian sedimentary rocks that comprise the lower strata of the central mound of Gale crater (Aeolis Mons, informally known as Mt. Sharp) and the surrounding plains (Aeolis Palus, informally known as the Bradbury Rise). The principal mineralogy of the sedimentary rocks is of basaltic composition, with evidence of post-depositional diagenetic overprinting. The rocks in many cases preserve much of their primary mineralogy and sedimentary features, suggesting that they were never strongly heated or deformed. Using aeolian soil composition as a proxy for the composition of the deposited and lithified sediment, it appears that, in many cases, the diagenetic changes observed are principally isochemical. Exceptions to this trend include secondary nodules, calcium sulfate veining, and rare Si-rich alteration halos. A surprising and yet poorly understood observation is that nearly all of the ~3.5 Ga sedimentary rocks analyzed to date contain 15–70 wt.% of X-ray amorphous material. Overall, this >800 m section of sedimentary rock explored in lower Mt. Sharp documents a perennial shallow lake environment grading upward into alternating lacustrine/fluvial and aeolian environments, many of which would have been habitable to microbial life.

A new organic mineral species, stanevansite, ideally Mg(C2H3O3)2·2H2O, was discovered from the western end of Pusch Ridge in the Santa Catalina Mountains (32° 21′ 42″ N, 110° 57′ 30″ W, at the elevation of 975 m), north of Tucson, Arizona, USA. It occurs as sprays of bladed crystals (up to 0.40 × 0.07 × 0.03 mm). Associated minerals include lazaraskeite, chrysocolla, malachite, wulfenite, mimetite, phosphohedyphane, cerussite, hematite, calcite, microcline, phlogopite, and quartz. Stanevansite crystals are colorless in transmitted light, transparent with white streak and vitreous luster. They are brittle and have a Mohs hardness of ∼1½; cleavage is perfect on {100}. Twinning is common on (100). The measured and calculated densities are 1.69(5) and 1.682 g/cm3, respectively. Optically, stanevansite is biaxial (+), with α = 1.539(5), β = 1.545(5), γ = 1.558(5), 2Vmeas. = 62(2)°, 2Vcal. = 69°. It is insoluble in water, but slowly dissolves in hydrochloric acid. An electron-microprobe analysis yielded an empirical formula, based on 8 O apfu and Σ(Mg + Zn) = 1 apfu, of (Mg0.95Zn0.05)Σ1.00(C2H3O3)2·2H2O, which can be simplified as (Mg,Zn)(C2H3O3)2·2H2O. Stanevansite is monoclinic with space group P21/c and unit-cell parameters a = 11.4927(2), b = 5.85470(10), c = 12.4711(2) Å, β = 91.1610(10)°, V = 838.96(2) Å3, and Z = 4. It is isostructural with several synthetic glycolate compounds having the general chemical formula M2+(C2H3O3)2·2H2O, where M2+ = Co2+, Mn, Zn, and Mg. The crystal structure of stanevansite is characterized by the mononuclear complex [Mg(C2H3O3)2(H2O)2], with such complexes being connected to one another by hydrogen bonds to form a three-dimensional supramolecular architecture. In a [Mg(C2H3O3)2(H2O)2] complex, Mg is octahedrally coordinated by two chelating glycolate ligands and two H2O molecules. Stanevansite represents the first hydrous glycolate mineral and is believed to have formed through the interaction of fluids containing glycolic acid (C2H4O3) derived from decaying plant materials or bacterial activities with Mg produced by the alteration of primary and secondary minerals. Its discovery, together with other glycolate minerals documented recently, namely lazaraskeite Cu(C2H3O3)2, jimkrieghite Ca(C2H3O3)2, and lianbinite (NH4)(C2H3O3)(C2H4O3), not only implies that more glycolate minerals may be found in nature, but also suggests that glycolate minerals may serve as a potential reservoir for biologically fixed carbon.

Two new organic minerals, alterite and magnesioalterite, ideally Zn 2 Fe 3 4 (SO 4 ) 4 (C 2 O 4 ) 2 (OH) 4 17H 2 O and Mg 2 Fe 3 4 (SO 4 ) 4 (C 2 O 4 ) 2 (OH) 4 17H 2 O, respectively, were discovered in carbonaceous petri fi ed wood from an unnamed uranium prospect, the Vermillion Cliffs, Coconino County, Arizona, USA. Associated minerals include gypsum, alunogen, natrojarosite, sulfur, celestine, and quartz. Both alterite and magnesioalterite are yellowish green in transmitted light and transparent with white streak and vitreous luster. They are brittle and have a Mohs hardness of 1.5; cleavage is perfect on (001). No parting or twinning was observed. The measured densities are 2.18(4) and 2.17(3) g/cm 3 for alterite and magnesioalterite, respectively. Optically, alterite is biaxial ( ), with a 1 / 4 1.545(5), p 1 / 4 1.565(5), y 1 / 4 1.635(5), 2 V meas. 1 / 4 56(2) degrees , 2 V cal. 1 / 4 58 degrees . Magnesioalterite is also biaxial ( ), with a 1 / 4 1.520 (5), p 1 / 4 1.578 (6), y 1 / 4 1.610 (5), 2 V meas. 1 / 4 74(2) degrees , 2 V cal. 1 / 4 76.5 degrees . Both new minerals are insoluble in water, but slowly dissolve in hydrochloric acid. An electron microprobe analysis, together with data from an Elemental Combustion System for C, yielded the empirical formula (based on 45 O apfu ) (Zn 0.84 Fe 2 0.57 Mg 0.48 Mn 0.14 ) epsilon 2.03 Fe 3 4.00 (S 0.99 O 4 ) 4 (C 2 O 4 ) 2 (OH) 4 1 7H 2 O for alterite and (Mg 0.74 Zn 0.60 Fe 2 0.58 Mn 0.09 ) epsilon 2.01 Fe 3 4.00 (SO 4 ) 4.00 (C 2 O 4 ) 2 (OH) 4 1 7H 2 O for magnesioalterite, both of which can be simpli fi ed to (Zn,Fe,Mg,Mn) 2 Fe 3 4 (SO 4 ) 4 (C 2 O 4 ) 2 (OH) 4 17H 2 O and (Mg,Zn, Fe 2 ,Mn) 2 Fe 3 4 (SO 4 ) 4 (C 2 O 4 ) 2 (OH) 4 17H 2 O, respectively. The measured 5 13 C % value for the carbonaceous petri fi ed wood on which the minerals were found is 23.1 and for alterite and magnesioalterite is 0.2. Alterite and magnesioalterite constitute a complete solid solution. They are monoclinic with the same space group, C 2 /c . The unit -cell parameters are a 1 / 4 16.7656(15), b 1 / 4 9.4074(7), c 1 / 4 25.351(3) angstrom, p 1 / 4 108.258(5) degrees , V 1 / 4 3797.1(6) angstrom 3 for alterite and a 1 / 4 16.7696(5), b 1 / 4 9.4020(2), c 1 / 4 25.3466(8) angstrom, p 1 / 4 108.2520(10) degrees , V 1 / 4 3795.28(18) angstrom 3 for magnesioalterite. The crystal structures of alterite and magnesioalterite are characterized by four-membered clusters of corner-sharing Fe 3 (O 5 OH) octahedra. These clusters are linked by SO 4 tetrahedra along the b axis and by the oxalate groups (C 2 O 4 ) 2 along the a axis to form sheets parallel to (001). Between the sheets are layers of M 2 (H 2 O) 6 octahedra ( M 1 / 4 Zn 2 , Mg 2 , Fe 2 , and Mn 2 ) and three symmetrically distinct H 2 O molecules that are not bonded to any non -H cations. The linkage between the sheets and the layers is achieved by hydrogen bonds, accounting for the good cleavage parallel to (001). Alterite and magnesioalterite are two of fi ve double -salt minerals with hydrated sulfate-oxalates, after coskrenite-(Ce), Ce 2 (SO 4 ) 2 (C 2 O 4 )8H 2 O; levinsonite-(Y), YAl(SO 4 ) 2 (C 2 O 4 )12H 2 O; and zugshunstite-(Ce), CeAl(SO 4 ) 2 (C 2 O 4 )12H 2 O. They are also the most hydrated among the 34 oxalate minerals reported thus far. Noticeably, both alterite and magnesioalterite contain a significant amount of Fe 2 substituting for Mg and Zn, pointing to the likelihood for the existence of a Fe 2 -analogue of alterite.

Gypsum is a common mineral at Gale crater on Mars, currently being explored by the Mars Science Laboratory (MSL) rover, Curiosity. In this paper, we summarize the associations of gypsum with other sulfate minerals (bassanite, anhydrite, jarosite, starkeyite, and kieserite) from the lowest levels of the crater’s northern moat zone (Aeolis Palus) up through ~0.8 km of the stratigraphic section in the lower slopes of the sedimentary mound developed around the central peak, Aeolis Mons (informally, Mount Sharp). The analysis is based on results from the CheMin X-ray diffraction instrument on Curiosity, supplemented with information from the rover’s versatile instrument suite. Gypsum does not occur with the same frequency as less hydrous Ca-sulfates, likely, in most cases, because of its dehydration to bassanite and possibly to anhydrite. All three of these Ca-sulfate phases often occur together and, along with other sulfates, in mixed assemblages that are evidence of limited equilibration on a cold, dry planet. In almost all samples, at least one of the Ca-sulfate minerals is present, except for a very limited interval where jarosite is the major sulfate mineral, with the implication of more acidic groundwater at a much later time in Gale crater’s history. Although observations from orbit reveal a sulfate-rich surface, currently active dark basaltic dunes at Gale crater have only small amounts of a single sulfate mineral, anhydrite. Gale crater has provided the most complete mineralogical analysis of a site on Mars so far, but the data in hand show that Gale crater mineralogy is not a blueprint with planet-wide application. The concurrent study of Jezero crater by the Mars 2020 mission and comparisons to what is believed to be the most extensive deposit of gypsum on Mars, in the dune fields at the north polar ice cap, show significant diversity. Unraveling the stories of gypsum and other sulfates on Mars is just beginning.

Eddavidite is a new mineral species (IMA2018-010) with ideal formula, Cu12Pb2O15Br2, and cubic Fm3¯m symmetry: a = 9.2407(9) Å; V = 789.1(2) Å3; Z = 2. Eddavidite is the bromine analog of murdochite, Cu12Pb2O15Cl2, with which it forms a solid solution series. The type locality is the Southwest mine, Bisbee, Cochise County, Arizona, U.S.A. Eddavidite also occurs in the Ojuela mine, Mapimí, Durango, Mexico. Eddavidite occurs as domains within mixed murdochite–eddavidite crystals. The empirical formula, normalized to 12 Cu apfu, is Cu12(Pb1.92Fe0.06Si0.06)(O15.08F0.02)-(Br0.99Cl0.89☐0.12). Type locality samples contain up to 67% eddavidite component, while Ojuela mine samples contain up to 62%. Mixed eddavidite–murdochite crystals show forms {100} and {111}; the habit grades from cubic through cuboctahedral to octahedral. Mixed eddavidite–-murdochite crystals exhibit good cleavage on {111}. Eddavidite is black, opaque with submetallic luster, and visually indistinguishable from intergrown murdochite. Its Mohs hardness is 4; dmeas. = 6.33 g/cm3, dcalc. = 6.45 g/cm3. The crystal structure, refined to R = 0.0112, consists of corner-sharing square planar CuO4 units, arranged in Cu12O24 metal oxide clusters, which encapsulate Br atoms. PbO8 cubes share edges with Cu12O24 clusters in a continuous framework. Eddavidite incorporates bromine remaining after desiccation of paleo-seawater at its two known localities, which were both once situated along the Western Interior Seaway.

A new mineral species, guangyuanite, ideally Pb3Cl3(Se4+O3)(OH), was discovered from the El Dragon mine, Antonio Quijarro Province, Potosi Department, Bolivia. It occurs as equant crystals. Associated minerals are Co-bearing krut'aite-penroseite, chalcomenite, schmiederite, olsacherite, phosgenite, anglesite, cerussite and franksousaite. Guangyuanite is pale yellow-brown in transmitted light, transparent with white streak and vitreous lustre. It is brittle and has a Mohs hardness of similar to 3. No parting or cleavage was observed. The calculated density is 7.63 g/cm(3). An electron microprobe analysis yielded an empirical formula [based on 7 (O + Cl) atoms per formula unit] of Pb3.02Cl3.01(Se0.994+O3)(OH), which can be simplified to Pb3Cl3(Se4+O3)(OH). Guangyuanite is isostructural with synthetic Pb3Cl3(Se4+O3)(OH). It is orthorhombic, with space group Pnma and unit-cell parameters a = 11.0003(5), b = 10.6460(5), c = 7.7902 angstrom, V = 912.31(6) angstrom 3 and Z = 4. The crystal structure of guangyuanite contains two symmetrically-distinct Pb (Pb1 and Pb2) cations, with Pb1 coordinated by eight anions (4O + 4Cl) and Pb2 only by six anions (3O + 3Cl), forming a marked lopsided coordination typical of Pb2+ with a stereochemically active 6s(2) lone electron pair. The Se4+ cation forms a typical [Se4+O3] trigonal pyramid. The crystal structure of guangyuanite can be described as consisting of layers of edge-sharing [Pb1O(4)Cl(4)] polyhedra parallel to (100). These layers are linked together by sharing polyhedral corners (Cl atoms), as well as [Pb2O3Cl3] and [Se4+O3] groups. Chemically, guangyuanite is one of six lead chloride selenite minerals reported thus far and closely related to orlandiite Pb3Cl4(Se4+O3)center dot H2O.

Powder X-ray diffraction (XRD) is a widely accepted technique for detecting trace asbestos content in solid samples. However, accurately quantifying asbestos concentrations below 0.5 wt% presents significant challenges with XRD alone. To address this limitation, we conducted a meticulous quantitative analysis using XRD on synthetic samples of talc-based powder spiked with varying amounts of natural tremolite and anthophyllite asbestos. At concentrations exceeding 0.5 wt%, both tremolite and anthophyllite displayed distinct XRD peaks. Yet, at lower concentrations (0.1 wt% and 0.05 wt%), the diffraction peaks of the contaminants became less prominent. To improve detection sensitivity, we explored different protocols of heavy liquid separation utilizing sodium polytungstate (SPT) to concentrate asbestos relative to the other mineral components. The optimized protocol, employing SPT with a density of 2.89 g/cm3, effectively separated amphibole asbestos from lighter, commonly associated minerals, like talc, clinochlore, and mica. Subsequent powder XRD analysis of the heavy fraction confirmed the successful removal of non-target materials, enhancing the diffraction peaks of tremolite and anthophyllite. Tremolite exhibited comparatively less weight loss than anthophyllite during this separation process. This study establishes the theoretical and practical viability of employing centrifugation in a heavy liquid to separate tremolite and anthophyllite from talc, providing valuable insights for asbestos detection and quantification in challenging scenarios.