Next Article in Journal
Ice-Jam Flooding of the Peace–Athabasca Delta, Canada: Insights from Recent Notable Spring Breakup Events and Implications for Strategic Flow Releases from Upstream Dams
Previous Article in Journal
Antipodal Seismic Observation and Sensitivity Kernel for the Liquid Region on the Earth’s Inner Core
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Geosciences
Volume 14
Issue 12
10.3390/geosciences14120334
geosciences-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

The Mobility of Major and Trace Elements in EOC Minerals on Parent Chondrite Bodies

by
Kristina Sukhanova
1,* and
Sergey Skublov
1,2
1
Institute of Precambrian Geology and Geochronology, Russian Academy of Sciences, 199034 St. Petersburg, Russia
2
Department of Mineralogy, Crystallography and Petrography, Empress Catherine II Saint Petersburg Mining University, 199106 St. Petersburg, Russia
*
Author to whom correspondence should be addressed.
Geosciences 2024, 14(12), 334; https://doi.org/10.3390/geosciences14120334
Submission received: 5 November 2024 / Revised: 27 November 2024 / Accepted: 3 December 2024 / Published: 6 December 2024
(This article belongs to the Section Geochemistry)
Browse Figures
Versions Notes

Abstract

The combined EPMA and SIMS study of the geochemical features of olivine, low-Ca pyroxene and plagioclase in equilibrated ordinary chondrites (EOCs) has revealed the effect of thermal metamorphism on trace element concentrations in EOC silicate minerals. In ordinary chondrites of petrological type 6, trace element composition is homogenized in olivine (Zr, Al, Ti, Ca, Cr, Sr and Ba) and low-Ca pyroxene (Zr, Hf, Y, Ti, Ca, Cr, Sr, Ba and Rb). Trace element concentrations in silicate minerals of petrological types 4 and 5 remain unequilibrated. Although variations in trace element concentrations have decreased, their concentrations in EOC minerals remain unchanged with an increase in the grade of thermal metamorphism. Plagioclase in equilibrated ordinary chondrites displays a consecutive decrease in trace element concentrations with a rise in the peak temperature of thermal metamorphism measured with an olivine-Cr spinel geothermometer. Chondrites of petrological type 4 show a metamorphic temperature of 670–682 °C, and meteorites of petrological type 5 reached equilibrium at a temperature of 687–700 °C. Chondrites of petrological type 6 show the highest metamorphic temperature of 734 °C. The temperatures are generally consistent with the concentric model of parent chondrite bodies.

1. Introduction

Ordinary chondrites are the most common type of meteorites, making up 87% of the Earth’s total meteoritic matter [1]. Chondrites are composed of chondrules, which are present as submillimetre-sized silicate spherules consisting mainly of olivine and pyroxene, with their interstices filled with recrystallized glass and mesostasis. Ordinary chondrites often show traces of thermal metamorphism, which took place on their parent bodies. Chondrites are divided into petrographic types 3–6, depending on the degree of their secondary processes. Type 3 is an unequilibrated chondrite, and type 6 is a highly processed chondrite. Ordinary chondrites of petrographic types 4–6 are called equilibrated chondrites (EOCs) [2].
Chondrites are divided into chemical groups H (high-iron), L (low-iron) and LL (low total and metallic iron concentration), depending on the metallic iron–total iron ratio. Groups L and LL contain more REE than H-chondrites [1].
Equilibrated ordinary chondrites are impacted by secondary processes on parent chondrite bodies, such as thermal and impact metamorphism, as well as fluid activity. Thermal metamorphism and fluid activity, which have affected the composition of all EOCs, provoked an increase in the grain size of the matrix minerals, the emergence of new mineral phases and the homogenization of olivine and low-Ca pyroxene composition [3]. Thus, EOC’s bulk composition values show that thermal metamorphism is an isochemical process relative to major elements (Ca, Mg, Al, Si, Fe, Ti) and REE [4] and that siderophile element concentrations decrease as the petrological type of chondrite (Cs, Bi, Cd, Br, In, Tl) [5] increases, indicating open system conditions on the parent body of chondrites. Fe, Mg [6,7] and Ca [8] concentrations in olivine and pyroxene and Cr and Ni concentrations in olivine [6,9,10] were homogenized due to the increasing diffusion rate of major elements under the oxidation conditions of thermal metamorphism. The mesostasis of EOC chondrules was recrystallized into plagioclase. This, together with the effect of fluids, triggered the removal of Si, Al, Na, K and REE into the matrix of chondrites and the emergence of phosphates [11,12,13].
Trace element concentrations in the silicate minerals of equilibrated ordinary chondrites have not yet been studied using local methods. The results of a few studies on unequilibrated ordinary chondrites (UOCs) show that trace elements in olivine and low-Ca pyroxene are sensitive to the conditions of their formation [14,15,16,17,18,19]. It has also been found that rare-earth element concentrations in olivine and low-Ca pyroxene in equilibrated chondrites are comparable, indicating crystallization under equilibrated element distribution conditions [20]. However, the available literature contains practically no evidence for variations in trace element concentrations provoked by thermal or impact metamorphism on parent chondrite bodies.
Local analysis of trace element concentrations in EOC’s olivine, low-Ca pyroxene and plagioclase is performed to assess the mobility of trace elements upon thermal metamorphism on parent chondrite bodies and to measure the degree of trace element homogenization. A representative collection of EOC, consisting of samples of seven meteorites—Kargapole (H4), Orlovka (H5), Saratov (L4), Elenovka (L5), Buschhof (L6), Bjurbole (L/LL4) and Knyahinya (L/LL5)—sent by collectors and by the Mining Museum at Empress Catherine II St. Petersburg Mining University, was compiled for the present study. Primary data on trace element mobility in the minerals of the above meteorites have already been reported [21,22,23,24,25]. In the present paper, the authors report the results obtained for all the above meteorites.
Mg and Fe diffusion rates and the heating temperatures of chondrite substance from 600 to 950 °C were measured due to the petrographic differences of chondrites and the gradual homogenization of olivine and pyroxene composition. As a result, an onion model of the parent chondrite bodies was constructed. The model is based on the concentric structure of a chondrite body, in which chondrites of petrological type 6 are as close as possible to the center of the body, and regolith-covered chondrites of type 3 are present on its surface [1].
The age-dates obtained for equilibrated ordinary chondrites are in agreement with the concentric model of parent bodies [26,27]. However, the cooling rate of chondrites, measured with various geothermometers, is not consistent with the data obtained [27,28].
To assess the effect of thermal metamorphism on trace element concentrations in the silicate minerals of EOC, the composition of Cr spinel was analyzed to calculate an olivine- Cr spinel thermometer using the relevant method [29].

2. Materials and Methods

In this study, the major element composition of minerals was determined using the electron probe micro analyzer (EPMA) at the Institute of Precambrian Geology and Geochronology Russian Academy of Sciences (IPGG RAS, St. Petersburg, Russia) on a Jeol JXA-8230. This electron probe microanalyzer was equipped with three wavelength dispersive spectrometers. Point measurements of mineral composition were performed at an accelerating voltage of 20 kV and a beam current of 20 nA for olivine and pyroxene and at a beam current of 10 nA for plagioclase. The focused beam was 3 μm in diameter. Natural minerals, as well as pure oxides and metals, were used as standards. To correct the matrix effect, the ZAF algorithm was used. The Kα1 lines were measured for all elements.
The contents of trace elements in silicate minerals were determined with secondary ion mass spectrometry (SIMS) using a Cameca IMS-4f ion microprobe at the Yaroslavl branch of the Institute of Physics and Technology (IPT) named after K.A. Valiev, Russian Academy of Sciences (Yaroslavl, Russia). The basics of the measurement technique corresponded to those reported in [30,31,32]. Prior to measurements, the mount was sputtered with gold. A survey was conducted employing this ion microprobe under the following conditions: a primary ion beam of O2−, beam diameter of 20 μm, ion current of 5–7 nA, and accelerating voltage of the primary beam of 15 kV. Positive secondary ions were collected from an area of 20 μm in diameter, limited by a field aperture. Molecular and cluster ions were energy filtered using an offset voltage of −100 V, with an energy window of 50 eV. Five counting cycles were carried out with a discrete transition between mass peaks within the given set. The accumulation time varied depending on signal intensity and was determined automatically by statistical control. The maximum counting time for any species in each cycle was 30 s. Counting time was dynamically corrected for each element and varied between 5 and 120 s depending on current counting statistics. Single analyses are averaged from three cycles of measurements. Total analysis time varied from 50 to 70 min.
The absolute concentrations of each element were calculated from the measured intensities of positive single-atom secondary ions, which were normalized to the intensity of secondary 30Si+ ions, using the relative sensitivity factors Ci = Ii/I30Si × i × CSiO2. Calibration curves were based on the measurements of the set of well-characterized standard samples [33]. The signals of 153Eu+, 174Yb+, 158Gd+, and 167Er+ were corrected to the interfering oxides of Ba and lighter REE in accordance with the scheme reported by Bottazzi et al. [34]. Glass KL-2G [33,35] and NIST-610 [36] were used as daily monitors for trace element analyses. Accuracy and precision were estimated to be better than 10% for all elements with contents above 1 ppm and 10% to 30% for contents of 0.1–1 ppm. The detection limit for almost all elements was about 0.01 ppm [32,37]. The trace element composition of rock-forming minerals was analyzed as close as possible to the analytical points for major elements using the EPMA method. The REE patterns of minerals were normalized to CI chondrite [38].

3. Results and Discussion

3.1. Major Element Mobility

Equilibrated ordinary chondrites consist mainly of olivine, low-Ca and/or high-Ca pyroxene and mesostasis, which is recrystallized into plagioclase in high petrological types.
Olivine is the most common silicate mineral occurring in all structural types of chondrules and in the matrix of meteorites. Olivine commonly occurs as idiomorphic or hypidiomorphic grains, no more than 1 mm in size (median size 300–500 µm). Olivine is occasionally overgrown with low- to high-Ca pyroxene.
An olivine phase is consistent with forsterite. Variations in Fo minal are dependent more on the chemical group of chondrites than on its petrological type and are in agreement with the relevant data available in the literature. Thus, olivine in meteorites of H-type is characterized by forsteritic minal with Fo of 78–80. Fo minal in meteorites of group L varies from 72 to 77, and in chondrites of group L/LL, olivine occurs as forsterite with minal 71–74. In this case, forsteritic minal varies to a smaller extent with the increase of the petrological type of chondrite.
Major and minor element concentrations practically do not vary with a petrological type. Variations in FeO and MgO in chondrites of petrological types 4 (23–17 wt.%, 42–37 wt.%, respectively) and 5 (23–17 wt.%, 42–37 wt.%, respectively) of petrological types remain the same but decrease in chondrites of petrological type 6 (22 wt.%, 38–37 wt.%, respectively).
Low-Ca pyroxene in equilibrated ordinary chondrites is present as idiomorphic and hypidiomorphic grains in the chondrules and matrix of meteorites. It holds second place after olivine in the abundance of silicate minerals. It often has high-Ca pyroxene rims. Pyroxene grains are commonly 200–300 µm in size.
Low-Ca pyroxene in EOC is consistent with enstatite, in which minal variations are characteristic of meteorites of petrological type 4 (Fs 14–25, Wo 0–4) but decrease in chondrites of petrological type 5 (Fs 16–24, Wo 0–4) and 6 (Fs 20–24, Wo 0–2). In this case, Fs minal becomes more abundant in the sequence H-L-LL and is dependent on the chemical group of chondrites.
Variations in practically all major and minor elements in low-Ca pyroxene decrease as the petrological type of chondrites increases. In this case, median FeO concentration in low-Ca pyroxene tends to increase (from 13.02 to 13.64 wt.%), as does the concentration of the minor elements CaO and TiO2 (from 0.48 to 0.77 wt.%, from 0.08 to 0.25 wt.%, respectively).
Plagioclase in EOC is commonly present as fine (50–200 µm) aggregates filling interstices between olivine and low-Ca pyroxene in the chondrules and matrix of meteorites. Plagioclase is present in all of the chondrites studied, but the Saratov meteorite also contains mesostasis. Plagioclase is present in all types of chondrules, but its aggregates in barred chondrules measure less than 20 µm—the size required for SIMS analysis. Plagioclase in chondrites of petrological types 4 and 5 is highly heterogeneous. It often contains micron-sized pyroxene and ore mineral grains. Plagioclase in a meteorite of petrological type 6 is completely homogeneous.
The phase composition of plagioclase in EOC is commonly highly heterogeneous within one meteorite. As a petrological type in plagioclase increases, median Al2O3 (from 14 to 21 wt.%), Na2O (from 5 to 9 wt.%) and K2O (from 0.63 to 1.13 wt.%) concentrations increase as well. MgO (from 4.28 to 0.12 wt.%), CaO (from 6.25 to 2.14 wt.%) and FeO (from 1.90 to 0.72 wt.%) concentrations in the plagioclase of chondrites decrease with a rise in petrological type.
Cr spinel is present in all of the meteorites studied, occurring commonly as separate grains in the matrix of chondrite or forming the external rim of chondrules. Cr spinel grains in meteorites of petrological type 4 are no more than 50 µm in size, but in chondrites of petrological types 5–6, they are up to 200 µm in size. They are commonly overgrown with metallic phases and troilite, but in Bjurbole meteorite, they form metallic chondrules.
Major and minor elements in Cr spinel from the EOC studied are invariably abundant. However, Cr spinel from Saratov meteorite is slightly enriched in Cr2O3 and ZnO and shows low Al2O3 concentration [39].
The petrographic description and composition of major elements in the silicate minerals of the equilibrated chondrites studied are consistent with the petrological type of the meteorite generally accepted in the international classification. However, Kargapole and Knyahinya meteorites display signs of vigorous impact metamorphism capable of disturbing the temperature equilibrium reached upon the thermal metamorphism of chondrites.
The temperature estimates at which equilibrium between olivine Cr spinel is reached indicate the peak of thermal metamorphism (see Table 1). Chondrites of petrological type 4 (Saratov and Bjurbole) show a metamorphic temperature of 670–682 °C, and meteorites of petrological type 5 (Orlovka, Elenovka and Knyahinya) reached equilibrium at a temperature of 687–700 °C. The only chondrite of petrological type 6 (Buschhof) shows the highest metamorphic temperature of 734 °C. The equilibrium temperatures of the olivine- Cr spinel geothermometer in the collection of EOC presented are generally consistent with the concentric model of parent chondrite bodies.
The only exception is the Kargapole meteorite, which shows an equilibrium temperature of 691 °C consistent with chondrites of 5th petrological type. This could be due to the disturbance of the equilibrium by impact metamorphism experienced by the meteorite. However, Knyahinya meteorite fits into the temperature range of chondrites of petrological type 5 and shows no petrographic signs of impact events in the sample studied, although the grade of impact metamorphism, described in the literature as S4 [39,40], is consistent with that of Kargapole meteorite. Obviously, impact metamorphism did not affect the Knyahinya meteorite’s composition. This assumption seems to be correct, considering the big size of the bolide and the fact that Knyahinya is the biggest meteorite in modern history.
The equilibrium temperatures of EOC are generally consistent with the concentric model of parent chondrite bodies, in which the most metamorphosed chondrites were in the center (Buschhof L6) of the body, less metamorphosed chondrites (Orlovka H5, Elenovka L5, Knyahinya L/LL5) in the middle and the least metamorphosed chondrites (Saratov L4, Bjurbole L/LL4) at the periphery of the body affected to a greater extent by impact events Kargapole H4) [21].

3.2. Trace Element Mobility

The presence of olivine in equilibrated ordinary chondrites indicates that its trace element concentrations are not dependent on the chemical group of chondrites. However, olivine in the Elenovka meteorite (L5) is poorer in refractory elements (Zr, Hf, Y and Al) than olivine in other chondrites.
The effect of thermal metamorphism on the abundance of practically all the trace elements analyzed in the olivine of EOC is indicated by less appreciable variations in their composition in meteorites of one petrological type. Thus, as the number of the petrological type of chondrite in olivine increases, Al, Zr, Ca, Ti, Sr, Cr, Ba, Rb and V concentrations are homogenized (Figure 1 and Figure 2).
In this case, the concentrations of all the above elements, except for V (Figure 1e) and Rb, remain equally unequilibrated in the chondrites of petrological types 4 and 5. Likewise, no variations in Hf, Y and REE concentrations, dependent on the number of the petrological type in the olivine of EOC, have been found (Figure 2).
Furthermore, Nb and Ni concentrations in olivine of petrological types 5 and 6 become more heterogeneous, and their Ce/Yb ratio exceeds that of olivine of petrological type 4.
In this case, EOC displays the well-defined positive correlations of refractory Nb/Zr (r = 0.76) and moderately volatile Cr/V (r = 0.96) elements (Figure 3). However, the diagram for these correlations shows no connection with a petrological type.
Despite the homogenization of the trace element composition in the olivine of the EOC, no change in the average level of trace element content, except for the depletion of Ca in the olivine of petrologic type 6, is observed.
The distribution spectra of trace elements in the olivine of the EOC do not demonstrate significant differences between the olivine of petrologic types 4, 5 and 6. The level of trace element content generally corresponds to the olivine of unequilibrated ordinary chondrites, with the exception of enrichment in LREE (Figure 4a). Insignificant enrichment in trace elements of olivine of the L group relative to olivine of other chemical groups of the EOC is also noted.
Low-Ca pyroxene in equilibrated ordinary chondrites of group L/LL contains more trace elements than pyroxene of groups H and L of EOC (Figure 4b).
Most of the trace elements studied in low-Ca pyroxene, like those in olivine, display smaller variations in abundance with an increase in the number of the petrological type of chondrite. Zr, Hf, Y, Ti, Ca, Cr, Sr, Ba and Rb concentrations in low-Ca pyroxene are gradually homogenized from petrological type 4 to type 6 in chondrites (Figure 5 and Figure 6). Al, V, Ni and REE concentrations reach their maximum in chondrites of petrological type 5 and decrease markedly in chondrites of petrological type 6 (Figure 6). Nb concentration in the low-Ca pyroxene of EOC shows a reverse trend, varying more markedly in chondrites of petrological types 5 and 6.
The homogenization of trace element composition in the low-Ca pyroxene of EOC does not affect their median concentration. Thus, Al, Hf, Y, Zr, Sr, Rb, Ba, V, Ni and REE concentrations remain at a similar level in chondrites of petrological types 4, 5 and 6. However, Ca and Cr concentrations in low-Ca pyroxene decrease markedly as the number of a petrological type increases, but Ti concentration in this sequence increases considerably.
Al and Rb (r = 0.79), Al and Eu (r = 0.72), V and HREE (r = 0.77), and V and Cr (r = 0.87) are directly correlated in low-Ca pyroxene from equilibrated ordinary chondrites (Figure 7). The above correlations are equally well-defined in the low-Ca pyroxene of all petrological types. However, the direct correlation of one element (Al, V), simultaneous with refractory (Eu, HREE) and moderately volatile (Rb, Cr) elements, cannot be reached upon direct gas-melt condensation, indicating the formation of chondritic material provoked by the melting of precursor minerals [16].
Trace element distribution spectra in low-Ca pyroxene are not indicative of any significant differences between the pyroxene of petrological types 4, 5 and 6 and the pyroxene of unequilibrated ordinary chondrites (Figure 8). The abundance of trace elements and the prevalence of HREE over LREE in ordinary chondrites of petrological types 4–6 are similar.
Trace element concentrations in the mesostasis of EOC chondrules are most heavily affected by thermal metamorphism. As a petrological type increases, trace element distribution in the glass and plagioclase of chondrites is homogenized, and the concentrations of practically all the elements analyzed decrease gradually.
However, plagioclase in chondrites of petrological type 5 displays the greatest variations in trace element (Hf, Nb, Y, Zr, Ti, Sr, Ba, Cr and V) concentrations, which decrease abruptly in plagioclase of petrological type 6 (Figure 8 and Figure 9). Only Rb and REE concentrations in the plagioclase of EOC (Figure 9c,d) are consecutively homogenized from petrological type 4 to type 6.
La/Sm and Ce/Yb ratios show a reverse sequence of rare-earth element homogenization, indicating greater variations in the plagioclase of EOC of petrological type 6 (Figure 9e,f).
Plagioclase in equilibrated ordinary chondrites of petrological types 4 and 5 shows that Zr and Yb are directly correlated (Figure 10d), indicating high Yb concentrations in plagioclase of petrological type 4. Plagioclase in chondrites of petrological type 6 displays no Zr/Yb correlation.
The plagioclase of EOC shows the direct correlation of incompatible elements Zr/Nb (r = 0.80), Ti/HREE (r = 0.94) and V/Cr (r = 0.89) (Figure 10). The diagrams of correlations show no relationship between trace element concentrations and the number of the petrological type of chondrite. However, the presence of separate EOC plagioclase grains markedly enriched in trace elements indicates the individual trace element enrichment of a certain chondrule.
Trace element distribution spectra in the plagioclase of EOC show no well-defined correlation of trace element concentration with the petrological type of chondrite (Figure 11a). However, trace element concentration tends to decrease consecutively from mesostasis and plagioclase of petrological type 4 to plagioclase of petrological type 5.
Plagioclase in Kargapole chondrite falls out of the sequence revealed, displaying low trace element concentrations due to the impact event in the meteorite’s record.
Elenovka meteorite has lower trace element concentrations in plagioclase than other meteorites of petrological type 5, suggesting its interaction with aquatic fluids.
EOC plagioclase of various chemical groups differs in the Rb/REE ratio (Figure 11b). In this case, the mesostasis of group L has high Rb concentrations, the plagioclase of group L/LL has the lowest concentrations, and the plagioclase of group H has intermediate concentrations. Plagioclase of all chemical groups displays a direct Sr/Ba correlation, but the EOC plagioclase of groups H and L lies on a common straight line, while the plagioclase of group L/LL contains low Sr and Ba concentrations.
Trace elements in the plagioclase of chondrites may be used for measuring high/low-temperature heating because their concentrations are clearly correlated with the temperature at which metamorphism was terminated. It is measured with an olivine-Cr spinel geothermometer. Thus, Saratov chondrite, showing signs of the weakest thermal metamorphism experienced by all the meteorites studied (670 °C), has preserved chondrule mesostasis in the form of glass. Orlovka and Bjurbole meteorites heated at 670–687 °C contain chondrule plagioclase occurring as plagioclase, which is similar in trace element distribution spectrum to plagioclase in Vigarano unequilibrated chondrite. Plagioclase in chondrites heated at a temperature above 670 °C is markedly depleted in trace elements and shows a positive europium anomaly, being more consistent with plagioclase in Renazzo unequilibrated carbonations chondrite.

4. Conclusions

Thus, thermal metamorphism on parent chondrite bodies provokes the homogenization of trace elements in olivine (Al, Ti, Zr, Ca, Sr, Cr, Ba) and pyroxene (Hf, Zr, Ti, Y, Ca, Sr, Ba, Cr, Rb) of petrological type 6 without affecting their distribution in chondrites of petrological types 4 and 5. Rare-earth elements Y and Hf in olivine remain nonhomogeneous in chondrites of petrological type 6. Thermal metamorphism does not affect trace element concentrations in the EOC’s olivine and pyroxene, except for Ca. Trace element concentrations in chondrule mesostasis decrease consecutively with an increase in the petrological type of chondrite.

Author Contributions

Conceptualization, S.S. and K.S.; methodology, S.S.; validation, K.S.; formal analysis, K.S.; investigation, K.S.; resources, S.S.; data curation, K.S.; writing—original draft preparation, K.S.; writing—review and editing, S.S.; visualization, K.S.; supervision, S.S.; project administration, K.S.; funding acquisition, S.S. All authors have read and agreed to the published version of the manuscript.

Funding

This study was supported by the government-financed research project FMUW-2022-0005 for the Institute of Precambrian Geology and Geochronology, Russian Academy of Sciences.

Data Availability Statement

Data are contained within the article.

Acknowledgments

The authors wish to thank S.G. Simakin and E.V. Potapov (YaF FTIAN) and O.L. Galankina (IPGG RAS) for analytical work.

Conflicts of Interest

The authors declare no conflicts of interest.

References

  1. Grady, M.; Pratesi, G.; Moggi-Cecchi, V. Ordinary Chondrite; Cambridge University Press: Cambridge, UK, 2014; p. 373. [Google Scholar]
  2. Dodd, R.T.; Hutchison, R. Meteorites: A Petrologic, Chemical and Isotopic Synthesis; Cambridge University Press: Cambridge, UK, 2004; p. 506. [Google Scholar]
  3. Scott, E.; Krot, A. Chondrites and Their Components. In Treatise on Geochemistry, Vol. 1: Meteorites and Cosmo-Chemical Processes; Davis, A., Ed.; Elsevier: Oxford, UK, 2014; Volume 1, pp. 65–137. [Google Scholar]
  4. Ali, A.; Nasir, S.J.; Jabeen, I.; Al Rawas, A.; Banerjee, N.R.; Osinski, G.R. Chemical and oxygen isotopic properties of ordinary chondrites (H5, L6) from Oman: Signs of isotopic equilibrium during thermal metamorphism. Meteorit. Planet. Sci. 2017, 52, 2097–2112. [Google Scholar] [CrossRef]
  5. Schaefer, L.; Fegley, B. Volatile element chemistry during metamorphism of ordinary chondritic material and some of its implications for the composition of asteroids. Icarus 2010, 205, 483–496. [Google Scholar] [CrossRef]
  6. Grossman, J.N.; Brearley, A.J. The onset of metamorphism in ordinary and carbonaceous chondrites. Meteorit. Planet. Sci. 2005, 40, 87–122. [Google Scholar] [CrossRef]
  7. Simon, S.B.; Sutton, S.R.; Grossman, L. The valence and coordination of titanium in ordinary and enstatite chondrites. Geochim. Cosmochim. Acta 2016, 189, 377–390. [Google Scholar] [CrossRef]
  8. Miyamoto, M.; McKay, D.S.; McKay, G.A.; Duke, M.B. Chemical zoning and homogenization of olivines in ordinary chondrites and implications for thermal histories of chondrules. J. Geophys. Res. 1986, 91, 12804–12816. [Google Scholar] [CrossRef]
  9. Frank, D.R.; Zolensky, M.E.; Le, L. Olivine in terminal particles of Stardust aerogel tracks and analogous grains in chondrite matrix. Geochim. Cosmochim. Acta 2014, 142, 240–259. [Google Scholar] [CrossRef]
  10. Friedrich, J.M.; Bridges, J.C.; Wang, M.-S.; Lipschutz, M.E. Chemical studies of L chondrites. VI: Variations with petrographic type and shock-loading among equilibrated falls. Geochim. Cosmochim. Acta 2004, 68, 2889–2904. [Google Scholar] [CrossRef]
  11. Lewis, J.A.; Jones, R.H. Phosphate and feldspar mineralogy of equilibrated L chondrites: The record of metasomatism during metamorphism in ordinary chondrite parent bodies. Meteorit. Planet. Sci. 2016, 51, 1886–1913. [Google Scholar] [CrossRef]
  12. Lewis, J.A.; Jones, R.H.; Garcea, S.C. Chondrule porosity in the L4 chondrite Saratov: Dissolution, chemical transport, and fluid flow. Geochim. Cosmochim. Acta 2018, 240, 293–313. [Google Scholar] [CrossRef]
  13. Murrell, M.; Burnett, D. The behavior of actinides, phosphorus, and rare earth elements during chondrite metamorphism. Geochim. Cosmochim. Acta 1983, 47, 1999–2014. [Google Scholar] [CrossRef]
  14. Alexander, C.D. Trace element contents of chondrule rims and interchondrule matrix in ordinary chondrites. Geochim. Cosmochim. Acta 1995, 59, 3247–3266. [Google Scholar] [CrossRef]
  15. Jacquet, E.; Alard, O.; Gounelle, M. Chondrule trace element geochemistry at the mineral scale. Meteorit. Planet. Sci. 2012, 47, 1695–1714. [Google Scholar] [CrossRef]
  16. Jacquet, E.; Alard, O.; Gounelle, M. Trace element geochemistry of ordinary chondrite chondrules: The type I/type II chondrule dichotomy. Geochim. Cosmochim. Acta 2015, 155, 47–67. [Google Scholar] [CrossRef]
  17. Ruzicka, A.; Floss, C.; Hutson, M. Relict olivine grains, chondrule recycling, and implications for the chemical, thermal, and mechanical processing of nebular materials. Geochim. Cosmochim. Acta 2008, 72, 5530–5557. [Google Scholar] [CrossRef]
  18. Varela, M.E.; Sylvester, P.; Brandstätter, F.; Engler, A. Nonporphyritic chondrules and chondrule fragments in enstatite chondrites: Insights into their origin and secondary processing. Meteorit. Planet. Sci. 2015, 50, 1338–1361. [Google Scholar] [CrossRef]
  19. Varela, M.E.; Sylvester, P.; Engler, A.; Kurat, G. Nonporphyritic chondrules from equilibrated Rumuruti and ordinary chondrites: Chemical evidence of secondary processing. Meteorit. Planet. Sci. 2012, 47, 1537–1557. [Google Scholar] [CrossRef]
  20. Dutta, A.; Bhattacharya, A.; Mishra, M.; Sadiq, M.; Roy, S. Trace elements and REE geochemistry of olivine and enstatite chondrules in ordinary chondrites: Insights into their cosmochemical genesis. In Proceedings of the 80th Annual Meeting of the Meteoritical Society, Santa Fe, NM, USA, 23–28 July 2017; p. 6088. [Google Scholar]
  21. Sukhanova, K.; Skublov, S.; Gavrilchik, A.; Galankina, O. Trace Elements in Silicate Minerals of the Kargapole Meteorite. Minerals 2023, 13, 368. [Google Scholar] [CrossRef]
  22. Sukhanova, K.G.; Kuznetsov, A.B.; Galankina, O.L. Features of olivine crystallization in ordinary chondrites (Saratov meteorite): Geochemistry of trace and rare earth elements. J. Min. Inst. 2022, 254, 149–157. [Google Scholar] [CrossRef]
  23. Sukhanova, K.G.; Kuznetsov, A.B.; Skublov, S.G. Geochemical Features of Chondrules from Orlovka Meteorite (H5): Evidence of Melting Precursors. Dokl. Earth Sci. 2022, 504, 28–33. [Google Scholar] [CrossRef]
  24. Sukhanova, K.G.; Skublov, S.G.; Galankina, O.L.; Obolonskaya, E.V.; Kotova, E.L. Trace element composition of silicate minerals in the chondrules and matrix of the Buschhof meteorite. Geochem. Int. 2020, 58, 1321–1330. [Google Scholar] [CrossRef]
  25. Sukhanova, K.G.; Skublov, S.G.; Galankina, O.L.; Obolonskaya, E.V.; Kotova, E.L. Trace element composition of silicate minerals in the porphyritic and nonporphyritic chondrules of Elenovka (L5) and Knyahinya (L/LL5) meteorites. Geochemistry 2020, 82, 125920. [Google Scholar] [CrossRef]
  26. Bouvier, A.; Blichert-Toft, J.; Moynier, F.; Vervoort, J.D.; Albarède, F. Pb–Pb dating constraints on the accretion and cooling history of chondrites. Geochim. Cosmochim. Acta 2007, 71, 1583–1604. [Google Scholar] [CrossRef]
  27. Kleine, T.; Touboul, M.; Van Orman, J.A.; Bourdon, B.; Maden, C.; Mezger, K.; Halliday, A.N. Hf–W thermochronometry: Closure temperature and constraints on the accretion and cooling history of the H chondrite parent body. Earth Planet. Sci. Lett. 2008, 270, 106–118. [Google Scholar] [CrossRef]
  28. Blackburn, T.; Alexander, C.M.O.D.; Carlson, R.; Elkins-Tanton, L.T. The accretion and impact history of the ordinary chondrite parent bodies. Geochim. Cosmochim. Acta 2017, 200, 201–217. [Google Scholar] [CrossRef]
  29. Wlotzka, F. Cr spinel and chromite as petrogenetic indicators in ordinary chondrites: Equilibration temperatures of petrologic types 3.7 to 6. Meteorit. Planet. Sci. 2005, 40, 1673–1702. [Google Scholar] [CrossRef]
  30. Portnyagin, M.; Almeev, R.; Matveev, S.; Holtz, F. Experimental evidence for rapid water exchange between melt inclusions in olivine and host magma. Earth Planet. Sci. Lett. 2008, 272, 541–552. [Google Scholar] [CrossRef]
  31. Nosova, A.; Narkisova, V.; Sazonova, L.; Simakin, S. Minor elements in clinopyroxene from Paleozoic volcanics of the Tagil island arc in the Central Urals. Geochem. Int. 2002, 40, 219–232. [Google Scholar]
  32. Batanova, V.; Suhr, G.; Sobolev, A. Origin of geochemical heterogeneity in the mantle peridotites from the Bay of Islands ophiolite, Newfoundland, Canada: Ion probe study of clinopyroxenes. Geochim. Cosmochim. Acta 1998, 62, 853–866. [Google Scholar] [CrossRef]
  33. Jochum, K.P.; Dingwell, D.B.; Rocholl, A.; Stoll, B.; Hofmann, A.W.; Becker, S.; Besmehn, A.; Bessette, D.; Dietze, H.J.; Dulski, P. The preparation and preliminary characterisation of eight geological MPI-DING reference glasses for in-situ microanalysis. Geostand. Newsl. 2000, 24, 87–133. [Google Scholar] [CrossRef]
  34. Bottazzi, P.; Ottolini, L.; Vannucci, R.; Zanetti, A. An accurate procedure for the quantification of rare earth elements in silicates. In SIMS 9th Proceedings; Wiley: New York, NY, USA, 1994; pp. 927–930. [Google Scholar]
  35. Jochum, K.P.; Stoll, B.; Herwig, K.; Willbold, M.; Hofmann, A.W.; Amini, M.; Aarburg, S.; Abouchami, W.; Hellebrand, E.; Mocek, B. MPI-DING reference glasses for in situ microanalysis: New reference values for element concentrations and isotope ratios. Geochem. Geophys. Geosyst. 2006, 7. [Google Scholar] [CrossRef]
  36. Rocholl, A.B.; Simon, K.; Jochum, K.P.; Bruhn, F.; Gehann, R.; Kramar, U.; Luecke, W.; Molzahn, M.; Pernicka, E.; Seufert, M. Chemical Characterisation of NIST Silicate Glass Certified Reference Material SRM 610 by ICP-MS, TIMS, LIMS, SSMS, INAA, AAS and PIXE. Geostand. Newsl. 1997, 21, 101–114. [Google Scholar] [CrossRef]
  37. Ottolini, L.; Bottazzi, P.; Vannucci, R. Quantification of lithium, beryllium, and boron in silicates by secondary-ion mass spectrometry using conventional energy filtering. Anal. Chem. 1993, 65, 1960–1968. [Google Scholar] [CrossRef]
  38. Palme, H.; Lodders, K.; Jones, A. Solar system abundances of the elements. In Planets, Asteriods, Comets and The Solar System. Vol. 2 of Treatise on Geochemistry, 2nd ed.; Davis, A.M., Ed.; Elsevier: Oxford, UK, 2014; Volume 2, pp. 15–36. [Google Scholar]
  39. Sukhanova, K.G.; Kuznetsov, A.B.; Skublov, S.G.; Galankina, O.L. Evaluation of thermal metamorphism temperature of equilibrated ordinary chondrites. Geodyn. Tectonophys. 2022, 13, 0618. [Google Scholar] [CrossRef]
  40. Bérczi, I.G.; Fürj, J.; Gucsik, A.; Nagy, S. Studies on petrography and shock stage of Nyírábrány LL5-chondrite from Hungary. Geochim. Cosmochim. Acta 2009, 55, 3845–3867. [Google Scholar]
Geosciences 14 00334 g001
Figure 1. Content variations of Zr (a), Al (b), Ti (c), Ca (d), Cr (e) and V (f) in olivine 4, 5 and 6 petrological types of EOC. The central line within each box represents the median concentration; boxes reflect interquartile ranges (25%–75%), while the whiskers indicate the range of values.
Figure 1. Content variations of Zr (a), Al (b), Ti (c), Ca (d), Cr (e) and V (f) in olivine 4, 5 and 6 petrological types of EOC. The central line within each box represents the median concentration; boxes reflect interquartile ranges (25%–75%), while the whiskers indicate the range of values.
Geosciences 14 00334 g001
Geosciences 14 00334 g002aGeosciences 14 00334 g002b
Figure 2. Content variations of Sr (a), Ba (b), Rb (c), Hf (d), Y (e) and REE (f) in olivine 4, 5 and 6 petrological types of EOC.
Figure 2. Content variations of Sr (a), Ba (b), Rb (c), Hf (d), Y (e) and REE (f) in olivine 4, 5 and 6 petrological types of EOC.
Geosciences 14 00334 g002aGeosciences 14 00334 g002b
Geosciences 14 00334 g003
Figure 3. Nb and Zr (a), Cr and V (b) variations (ppm) in olivine from EOC.
Figure 3. Nb and Zr (a), Cr and V (b) variations (ppm) in olivine from EOC.
Geosciences 14 00334 g003
Geosciences 14 00334 g004
Figure 4. CI chondrite-normalized trace element patterns of olivine (a) and low-Ca pyroxene (b) from EOC.
Figure 4. CI chondrite-normalized trace element patterns of olivine (a) and low-Ca pyroxene (b) from EOC.
Geosciences 14 00334 g004
Geosciences 14 00334 g005aGeosciences 14 00334 g005b
Figure 5. Content variations of Zr (a), Hf (b), Ti (c), Y (d), Sr (e) and Rb (f) in low-Ca pyroxene 4, 5, and 6 petrological types of EOC.
Figure 5. Content variations of Zr (a), Hf (b), Ti (c), Y (d), Sr (e) and Rb (f) in low-Ca pyroxene 4, 5, and 6 petrological types of EOC.
Geosciences 14 00334 g005aGeosciences 14 00334 g005b
Geosciences 14 00334 g006
Figure 6. Content variations of Ca (a), Cr (b), Al (c), REE (d), V (e) and Ni (f) in low-Ca pyroxene 4, 5 and 6 petrological types of EOC.
Figure 6. Content variations of Ca (a), Cr (b), Al (c), REE (d), V (e) and Ni (f) in low-Ca pyroxene 4, 5 and 6 petrological types of EOC.
Geosciences 14 00334 g006
Geosciences 14 00334 g007
Figure 7. HREE/V (a), Rb/Al (b), Cr/V (c) and Eu/Al (d) variations (ppm) in low-Ca pyroxene from EOC.
Figure 7. HREE/V (a), Rb/Al (b), Cr/V (c) and Eu/Al (d) variations (ppm) in low-Ca pyroxene from EOC.
Geosciences 14 00334 g007
Geosciences 14 00334 g008
Figure 8. Content variations of Zr (a), Y (b), Ti (c), Nb (d), Sr (e) and Ba (f) in plagioclase 4, 5 and 6 petrological types of EOC.
Figure 8. Content variations of Zr (a), Y (b), Ti (c), Nb (d), Sr (e) and Ba (f) in plagioclase 4, 5 and 6 petrological types of EOC.
Geosciences 14 00334 g008
Geosciences 14 00334 g009
Figure 9. Content variations of Cr (a), V (b), Rb (c), REE (d), La/Sm (e) and Ce/Yb (f) in plagioclase 4, 5 and 6 petrological types of EOC.
Figure 9. Content variations of Cr (a), V (b), Rb (c), REE (d), La/Sm (e) and Ce/Yb (f) in plagioclase 4, 5 and 6 petrological types of EOC.
Geosciences 14 00334 g009
Geosciences 14 00334 g010
Figure 10. Cr/V (a), Yb/Zr (b), HREE/Ti (c) and Nb/Zr (d) variations (ppm) in plagioclase from EOC.
Figure 10. Cr/V (a), Yb/Zr (b), HREE/Ti (c) and Nb/Zr (d) variations (ppm) in plagioclase from EOC.
Geosciences 14 00334 g010
Geosciences 14 00334 g011
Figure 11. CI chondrite-normalized trace element patterns of plagioclase (a) and REE and Rb variation (ppm) in plagioclase (b) from EOC.
Figure 11. CI chondrite-normalized trace element patterns of plagioclase (a) and REE and Rb variation (ppm) in plagioclase (b) from EOC.
Geosciences 14 00334 g011
Table 1. Average composition (wt.%) of Cr spinel and olivine in EOC.
Table 1. Average composition (wt.%) of Cr spinel and olivine in EOC.
MeteoriteMineralSiO2Al2O3MgOTiO2NiOFeOMnOCr2O3V2O3ZnOTotalT, °C
Kargapole (H4)Cr-Spl0.075.942.872.08b.d.l.28.290.9058.880.640.3199.98691
Ol39.32b.d.l.42.13b.d.l.b.d.l.17.530.45b.d.l.n.d.n.d.99.42
Orlovka (H5)Cr-Spl0.196.222.832.00b.d.l.28.710.9158.600.670.41100.53687
Ol39.48b.d.l.41.72b.d.l.b.d.l.17.660.46b.d.l.n.d.n.d.99.32
Saratov (L4)Cr-Spl0.143.601.701.51b.d.l.30.190.7961.310.720.50100.46670
Ol38.56b.d.l.38.840.06b.d.l.21.700.47b.d.l.n.d.n.d.99.63
Elenovka (L5)Cr-Splb.d.l.5.262.072.93b.d.l.30.660.7357.560.710.33100.26691
Ol38.63b.d.l.37.99b.d.l.b.d.l.22.690.48b.d.l.n.d.n.d.99.79
Buschhof (L6)Cr-Splb.d.l.5.382.642.84b.d.l.29.880.6957.850.640.26100.17734
Ol38.43b.d.l.38.24b.d.l.b.d.l.22.610.470.07n.d.n.d.99.82
Bjurbole (L/LL4)Cr-Spl0.125.391.861.930.0630.770.7058.590.660.37100.45682
Ol38.79b.d.l.37.560.05b.d.l.23.870.47b.d.l.n.d.n.d.100.75
Knyahinya (L/LL5)Cr-Spl0.055.582.222.55b.d.l.30.380.7257.420.670.2699.84700
Ol37.89b.d.l.38.03b.d.l.b.d.l.22.560.46b.d.l.n.d.n.d.98.94
Note. b.d.l.—below detection limit, n.d.—not detected.
Disclaimer/Publisher’s Note: The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.

Share and Cite

MDPI and ACS Style

Sukhanova, K.; Skublov, S. The Mobility of Major and Trace Elements in EOC Minerals on Parent Chondrite Bodies. Geosciences 2024, 14, 334. https://doi.org/10.3390/geosciences14120334

AMA Style

Sukhanova K, Skublov S. The Mobility of Major and Trace Elements in EOC Minerals on Parent Chondrite Bodies. Geosciences. 2024; 14(12):334. https://doi.org/10.3390/geosciences14120334

Chicago/Turabian Style

Sukhanova, Kristina, and Sergey Skublov. 2024. "The Mobility of Major and Trace Elements in EOC Minerals on Parent Chondrite Bodies" Geosciences 14, no. 12: 334. https://doi.org/10.3390/geosciences14120334

APA Style

Sukhanova, K., & Skublov, S. (2024). The Mobility of Major and Trace Elements in EOC Minerals on Parent Chondrite Bodies. Geosciences, 14(12), 334. https://doi.org/10.3390/geosciences14120334

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop