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4 June 2018

Chemical-Petrographic Types and Shock Metamorphism of 184 Grove Mountains Equilibrated Ordinary Chondrites

,
and
1
Institute of Geology, Hunan University of Science and Technology, Xiangtan 411201, China
2
Hunan Provincial Key Laboratory of Shale Gas Resource Utilization, Xiangtan 411201, China
*
Author to whom correspondence should be addressed.
Minerals2018, 8(6), 240;https://doi.org/10.3390/min8060240
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Abstract

We reported the petrography and mineral chemistry of 184 equilibrated ordinary chondrites collected from Grove Mountains, Antarctica. The chemical-petrographic types and shock metamorphism degrees of these chondrites were assigned. They were classified into 46 H groups (22 H4, 20 H5, and four H6), 133 L groups (eight L4, 75 L5, and 50 L6), and five LL groups (four LL4 and one LL5). Some of these chondrites could be paired; however, both H and L group meteorites were affected. Further studies such as terrestrial ages and thermal luminescence are required in order to confirm the pairings. The relative abundances of H, L, and LL are different in Grove Mountain meteorites, when compared to those in Transcontinental Ridge meteorites. Based on the shock effects, the shock metamorphism degrees of these chondrites were assigned. Compared to previous studies, the heavily shocked samples of S4 and S5 have a higher fraction (59 out of 184) in Grove Mountain ordinary chondrites. The L group (54 out of 59) is the dominant chemical group in the heavily shocked chondrites, except for five meteorites which belong to the H group. The shock metamorphism degrees of the H and L groups are distinct, which may indicate different surface properties in their parent bodies. In addition, the petrologic types and shock degrees are probably closely related, with the most heavily shocked chondrites observed in types 5 and 6.

1. Introduction

Since the first discovery of nine meteorites of different chemical groups in the Yamato area, Antarctica by a Japanese team in 1969, Antarctica has become the most meteorite-rich region in the world. Many rare types of meteorites have been found in Antarctica, e.g., Martian meteorites, Lunar meteorites, and carbonaceous chondrites. The Grove Mountains consist of 64 nunataks, which are located in eastern Antarctica [1]. During the 15th Chinese Antarctic exploration between 1998 and 1999, a Chinese team conducted their first field survey of the Grove Mountains. More than 10,000 meteorites were collected by the Chinese Antarctic Research Expedition (CHINARE) in this area (Figure 1).
Figure 1. Map of meteorite concentration sites in Antarctica (based on the literature [14]). The red dots, blue dots, and green dots represent the meteorite enrichment areas found by China, the United States, and Japan and other countries, respectively.
With a large number of Antarctica meteorites found, some comparative studies could be conducted, e.g., the type and mass distribution patterns and shock metamorphism in different chemical and petrographic chondrite types. Previously, some studies showed that there is no close connection between the distribution patterns of the types and mass, and the sites where the meteorites are collected [2,3,4]. On the other hand, some large meteorite showers have been evidenced in Antarctica. Locally, these showers do result in establishing a connection between meteorite types, mass, and sites [5]. Shock metamorphism from hypervelocity collisions is the most common feature of meteorite parent bodies. Deformation, melting, and the decomposition of mineral components are recorded under shock effects [6,7]. Moreover, natural high-pressure polymorphs of rock-forming minerals were also discovered in heavily shocked meteorites [6,7,8,9,10]. Since the high pressures and temperature conditions during shock events are comparable to those of the Earth’s transition zone or of the lower mantle, the study of shock effects in meteorites is of great importance for deciphering the collisional and geological history of their asteroidal parent bodies [11,12]. Based on the shock effects in silicate minerals and shock-induced localized melting in ordinary chondrites, seven degrees of shock metamorphism (S1–S6 and shock melted) were classified by Stőffler et al.; the Pressure-Temperature (P-T) conditions of every shock degree were also given in their study [13].
In order to compare the type distribution patterns and shock metamorphism degrees with different chemical-petrographic types in chondrites, 184 equilibrated ordinary chondrites were randomly selected for classification. In this paper, the petrography and mineral chemistry of these meteorites are reported, and their chemical-petrographic types and shock metamorphism degrees are assigned.

2. Samples and Experiments

Samples of these meteorites were embedded in epoxy, and then cut into <1 mm thin slices with a low-speed diamond saw. They were prepared to standard polished thin sections without water. Textural observations of these chondrites were studied using an optical microscope and a back-scattered electron (BSE) image model of a JEOL 8100 electronic probe microanalyzer (EPMA) (Tokyo, Japan) at the Guangzhou Institute of Geochemistry, Chinese Academy of Sciences. Quantitative analyses for silicates were carried out using the same EPMA with a 15 keV accelerating voltage and a 20 nA beam current. Natural and synthetic minerals were used as standards. An X-ray peak deconvolution program was applied to correct for the Kα lines of V and Mn by the Kβ lines of Ti and Cr. Analytical results of the silicates ware corrected by the ZAF method. Modal contents of opaque mineral (metallic Fe-Ni and troilite) were calculated from areas of the phase in BSE images of the polished thin sections. Chemical-petrographic types of these chondrites are mainly based on References [15,16,17], and their shock metamorphism results are based on Reference [13].

3. Chemical-Petrographic Types

The basic characteristics of these Grove Mountains chondrites are summarized in Table A1, including chemical-petrographic types, found location, mass, opaque mineral (vol %), mineral chemistry, and shock metamorphism. They are all equilibrated, including 46 meteorites classified as H chondrites (22 H4, 20 H5, and four H6), 133 L chondrites (eight L4, 75 L5, and 50 L6), and five LL chondrites (four LL4 and one LL5).
All 184 meteorites have homogenized mineral chemistry and their matrices are recrystallized (Figure 2). This indicates that they experienced significant thermal metamorphism in their parent bodies. Type 5 and 6 chondrites have blurred outlines of chondrules (Figure 2c,d), but chondrules are clearly outlined in type 4 (Figure 2a,b). The PMD (percent mean deviation) value of the Fa (Fayalite) content of olivine in all chondrites is most <5%. Low-Ca pyroxene is also homogeneous in most of these chondrites, with a PMD of Fs (ferrosilite) content <5%. The Fa content of olivine and Fs content of low-Ca pyroxene of these meteorites are plotted in Figure 3.
Figure 2. Back-scattered electron (BSE) images of representative equilibrated ordinary chondrites. (a) GRV 020008 (H4); (b) GRV 020038 (L4); (c) GRV 022178 (L6); (d) GRV 020041 (LL4). Ol—olivine, Px—pyroxene, OM—opaque mineral.
Figure 3. Fa of olivine and Fs of low-Ca pyroxene of 184 chondrites.

3.1. Group H

There are 46 meteorites in this group (Table A1). The Fa values of olivine for all chondrites range from 17.0 to 21.0 mol %, and the Fs values of low-Ca pyroxene range from 15.4 to 18.5 mol %. Both the Fa and Fs tally with the ranges of the H group (Figure 3). These 46 meteorites experienced significant thermal metamorphism. Twenty-two meteorites (Table A1) have a homogenized mineral chemistry and clear outlines of chondrules. Additionally, their fine-grained matrices are partly recrystallized (Figure 2a), with the sizes of the recrystallized matrices being 5–15 μm. Brown-colored glass was found in a few chondrules. Accordingly, these meteorites belong to H4. The outlines of the chondrules in 20 chondrites (Table A1) can been recognized. Additionally, their matrices are well recrystallized, with the sizes of these grains being 10–40 μm. Secondary feldspar within the matrix and chondrules is popular, with sizes ranging from 10–50 μm. These 20 chondrites were assigned to H5. They were identified as GRV 020072, 020093, 020098, and 021522, having similar petrographic characteristics. Additionally, their matrices are intensely recrystallized, with the sizes of these grains being 50–150 μm. The chondrules in these meteorites are hard to locate, with only a few fragments remaining. These chondrites belong to type H6.

3.2. Group L

One hundred and thirty-three meteorites belong to the L group, and they are equilibrated (Table A1). The Fa values of olivine in all the chondrites range from 23.0 to 26.7 mol %, and the Fs values of low-Ca pyroxene range from 18.2 to 22.8 mol %. Both Fa and Fs values are within the ranges of the group L (Figure 3). These chondrites (GRV 020038, 020049, 021643, 021654, 021668, 021726, 021800, and 022221) have a homogenized mineral chemistry and clear outlines of chondrules. Additionally, their fine-grained matrices are only partly recrystallized (Figure 2b), with the sizes of the recrystallized matrices being 5–10 μm. The primary glass was found in a few chondrules. This indicates that these meteorites experienced the lowest degree of thermal metamorphism. However, all eight chondrites can be assigned to type L4. In 75 meteorites (Table A1), many chondrules are fractured and occur as fragments, but they can be recognized. The matrices of these chondrites are well recrystallized (20–40 μm), with plagioclase being commonly observed. These meteorites belong to L5. The other 50 meteorites (Table A1) were assigned to type L6. Additionally, their matrices were intensely recrystallized, with the sizes of these grains being 50–200 μm. Only a few fragments of chondrules can be found (Figure 2c).

3.3. Group LL

Only five chondrites were assigned to this group (Table A1), i.e., GRV 020019, 020021, 020028, 020037, and 020041. The modal abundances of the opaque mineral (0.6–4.1 vol %), along with the compositions of olivine (mean Fa: 27.5–31.6 mol %) and low-Ca pyroxene (mean Fs: 23.1–27.2 mol %), indicate that these meteorites belong to the LL group. GRV 020019 experienced a much stronger thermal metamorphism than the other four meteorites. In GRV 020019, only a few chondrules could be readily recognized. In contrast, in GRV 020021, 020028, 020037, and 020041, the chondrules are clearly outlined (Figure 2d), with their matrices being only partly recrystallized (Figure 2d), and with the sizes of these matrices being 5–20 μm. Brown-colored glass was found in a few chondrules. Therefore, GRV 020021,020028, 020037, and 020041 were classified as LL4, and GRV 020019 as LL5.

4. Discussion

4.1. Type and Mass Distribution Patterns

Based on the statistics of the classified 184 equilibrated ordinary chondrites, the relative abundances of H, L, and LL groups were 25%, 72.3%, and 2.7%, respectively. The relative abundance of L chondrites was as high as by a factor of ~2.9 of the H group, while the LL chondrites were rather few in number. Figure 4 shows the type distribution patterns of the Grove Mountain meteorites in this paper when compared with those of Transcontinental Ridge meteorites [16]. The abundance ratio of H:L:LL was 25:72.3:2.7 for meteorites from the Grove Mountains, which is different from that of the Transcontinental Ridges (42:48:10) [16]. It is clear that the Grove Mountain chondrites have a higher abundance of the L chemical group and less H and LL groups when compared with the Transcontinental Ridge chondrites.
Figure 4. Comparison of the distribution patterns of the chondrite chemical groups between the Transcontinental regions and the Grove Mountains.
The Grove Mountain meteorites have smaller sizes (average mass of 67.9 g) when compared with the Transcontinental Ridge meteorites (average mass of 261.3 g) [16]. The abundance of Grove Mountain meteorites decreases exponentially with the increase of mass. Tiny meteorites (mass < 25 g) are more than 50%. Many Grove Mountain meteorites are small fragments that were found very close to one another. Therefore, they are probably broken pieces from some larger meteorites. On the other hand, the field team in the Grove Mountains searched for meteorites by foot, finding meteorites as small as 0.1 g, while blue ices along the Transcontinental Ridges were swept with a skidoo or snowmobile.
Because of the transfer and concentration of meteorites by glacier and wind, the meteorites collected from the same region in Antarctica face two possibilities: (1) each piece belongs to individual fall events, or (2) some of them may be pieces of the same meteorite fall (meteorite shower, or paired meteorites) [5,16]. Different search methods were employed between the Grove Mountains (by foot) and the Transcontinental Ridges (skidoo), so smaller meteorites could be found in the Grove Mountains. As discussed above, the abundance ratio of L:H was ~2.9; thus, it is obvious that the Grove Mountains have a greater L group presence and a lower H group presence when compared with the Transcontinental Ridges. The abundance ratio of L:H was ~5.6 (Table A1) if we limit ourselves to Grove Mountains meteorites with a mass >10 g. Therefore, the higher H:L ratio in the Grove Mountains is not related to the mass. Both H and L group meteorites were affected, whether they were from a meteor shower or pieces broken from some larger meteorites. In this paper, we reported the petrography and mineral chemistry of 184 equilibrated ordinary chondrites. However, further studies such as terrestrial ages and thermal luminescence are required in order to confirm the pairing.

4.2. Shock Metamorphism

A petrographic classification of shock metamorphism degrees of ordinary chondrites was put forward by Stőffler et al. [13] and has since been widely used [16,17,18,19]. According to their classification, seven shock metamorphism degrees (S1–S6 and shock melted) were defined, based on the shock effects in the main silicate components, as recognized by thin section microscopy. The characteristic shock effects of each shock degree are (Table 1): S1 (unshocked)—sharp optical extinction of olivine; S2 (very weakly shocked)—undulatory extinction of olivine; S3 (weakly shocked)—planar fractures in olivine; S4 (moderately shocked)—mosaicism in olivine; S5 (strongly shocked)—isotropization of plagioclase (maskelynite) and planar deformation features in olivine; and S6 (very strongly shocked—recrystallization of olivine, sometimes combined with phase transformations (ringwoodite and/or phases produced by dissociation reactions). S6 effects are always restricted to regions adjacent to melted portions of a sample which is otherwise only strongly shocked [13]. With the development of high-pressure experiments and study in shock metamorphism in meteorites, modifications and corrections were made on the Pressure-Temperature-time (P-T-t) conditions and formation history of high-pressure minerals in meteorites [11,20,21,22]. Accordingly, modifications and revisions are needed for the current classification and pressure calibration system of shock degrees in ordinary chondrites (Table 1). In this study, we classified the shock degrees of 184 Grove Mountain ordinary chondrites (see Table A1 and Table 1). The shock metamorphism degrees of the 184 chondrites are S1 (10 meteorites), S2 (61 meteorites), S3 (54 meteorites), S4 (54 meteorites), and S5 (five meteorites) (Figure 5), respectively.
Table 1. Shock metamorphism degrees of Grove Mountains chondrites (based on the literature [13]).
Figure 5. (a) Photomicrograph of olivine in GRV 020069 (S2) under cross-polarized light. The grey-colored grain in the center of the view exhibits undulatory extinction. (b) Photomicrograph of olivine in GRV 022244 (S3) under cross-polarized light. The grain of olivine has two sets of planar fractures. (c) Photomicrograph of shock-induced vein in GRV 020125(S4) under plane-polarized light. Some silicate clasts can be found in vein. (d) Photomicrograph of shock-induced vein in GRV 022194(S5) under plane-polarized light. Melt pockets and shock veins are pervasive.
Figure 6 shows the statistic results of the shock metamorphism degrees within different chemical groups and petrologic types of these Grove Mountain chondrites. Due to its low abundance, the LL group was not considered. The H and L groups displayed distinct abundance patterns. Specifically, 41% of L chondrites were heavily shocked (S4–5) with an occurrence of shock-induced melt veins, while the shock metamorphism is not so extensively developed in H group chondrites. Most H chondrites were weakly shocked, with only four meteorites classified as S4 (Figure 6a).
Figure 6. Histograms of shock degrees of Grove Mountain chondrites: (a) chemical groups, and (b) petrographic types.
Stőffler et al. studied the shock metamorphism in 35 H group, 27 L group, and 14 LL group chondrites. Their results showed that the differences in the frequency distribution of shock degrees in H, L, and LL groups are minor; besides, the shock effects and the sequence of progressively increasing degrees of shock metamorphism are very similar [13]. However, the investigation of the Meteoritical Bulletin Database suggests that the frequency distributions of shock degrees between L and H groups are different [11]. There are 23 L group out of all the chondrites that are shocked to S4–S6, whereas the number of H groups is nine. It is evident that the L group chondrites have experienced a stronger shock metamorphism than those of the H group [23], which is consistent with the results in this study (Figure 6a).
Since different groups of chondrites come from different parent bodies, the diverse distribution of frequencies of shock degrees between H and L groups may result from the different physical properties of the surfaces of their parent bodies [24]; for example, the thickness of the soil layer, the petrologic rock type on the surface, etc. As discussed above, a thick and porous regolith is not favorable to reserving high pressure and temperature conditions. An analogous case can be seen on the moon and on Mars. The former is covered by a layer of lunar regolith 2–10 m in depth, while Martian soil is not so abundant on the surface of Mars. Therefore, Martian meteorites have experienced a stronger shock metamorphism than the lunar meteorites [11,25,26,27,28,29,30,31,32].
Another aspect is that the frequency of shock degrees within different petrologic types (Figure 6b) reveals some variations. With increasing petrologic types, the frequency of the shock degrees S3, S4, and S5 increases. The shock degree S2 is the most abundant in type 4 meteorites, while the shock degrees S2 and S4 are the most abundant in type 5 meteorites, and S3 and S4 are the most abundant in type 6 meteorites. There is a lack of shock degrees S1 and S5 in petrologic type 6 and 4 meteorites, respectively. Stöffler et al. made the same observation: no S5 and S6 degrees were observed among type 4 ordinary chondrites [23]. The tendency that, between petrologic types and shock degrees, heavily shocked samples are most likely to be observed in highly petrologic chondrite types may be attributed to the different physical properties of all chondrite types in their unshocked state. High equilibrated samples (type 5/6 chondrites) are essentially coherent nonporous rocks, in which the high pressures and temperatures are more easily retained for a longer time during a shock event, while type 4 chondrites are more porous and richer in volatiles which are more easily crushed upon impact, thereby releasing the high pressure.

5. Conclusions

We studied the petrography and mineral chemistry of 184 Grove Mountain equilibrated ordinary chondrites. Their chemical-petrographic types were assigned, including 46 H groups (22 H4, 20 H5, and four H6), 133 L groups (eight L4, 75 L5, and 50 L6), and five LL groups (four LL4 and one LL5). Some of these chondrites could be paired; however, both H and L group meteorites were affected.
The relative abundances of H, L, and LL are different for Grove Mountain meteorites when compared with those of Transcontinental Ridge meteorites. The Grove Mountain meteorites have smaller sizes (average mass of 67.9 g) in comparison with the latter meteorites (average mass of 261.3 g).
On the basis of the observed shock effects, the shock degrees of the 184 ordinary chondrites were classified. There are 10 with an S1 shock degree, 61 with S2, 54 with S3, 54 with S4, and five with S5. A comparison of the frequencies of shock degrees within different chemical groups shows a diverse frequency distribution of shock degrees between H and L groups, which may represent the difference between the physical properties of their parent body surfaces. Besides, it appears that the frequency of the shock degrees S3, S4, and S5 increases with increasing petrologic types.

Author Contributions

D.D. conceived and designed the experiments; D.D. and S.L. performed the experiments; D.D., S.L. and X.L. analyzed the data; D.D. wrote the paper, assisted by all other authors.

Funding

This research was funded by the National Natural Science Foundation of China (41673070 and 41503062).

Acknowledgments

Three anonymous reviewers are thanked for their constructive comments and suggestions which greatly improved the quality of this paper. We thank the Polar Research Institute of China for providing all of the samples in this study. The EPMA analysis of 92 meteorites were conducted by Dr. Shijie Li.

Conflicts of Interest

The authors declare no conflict of interest.

Appendix A

Table A1. The major characteristics of 184 ordinary chondrites.
Table A1. The major characteristics of 184 ordinary chondrites.
MeteoritesFound LocationTypeWeight (g)Opaque Mineral (vol%)OlivineLow-Ca PyroxeneShock Degrees
FaPMDFsPMD
GRV020007S73°05′23′′ E75°11′22′′H425.98.417.03.815.83.7S2
GRV020008S73°05′05′′ E75°12′33′′H46.24.518.01.116.11.6S2
GRV020042S73°00′23′′ E75°11′32′′H42.24.218.21.616.22.6S1
GRV020051S72°59′30′′ E75°13′40′′H41.44.019.51.217.42.1S2
GRV020066S72°59′57′′ E75°14′20′′H41.83.317.44.116.54.7S1
GRV020070S72°59′57′′ E75°12′10′′H47.96.018.40.816.41.6S3
GRV020074S72°59′45′′ E75°12′35′′H41.58.419.96.417.54.0S3
GRV020088S73°00′13′′ E75°15′10′′H43.05.118.61.717.01.3S2
GRV020091S72°59′45′′ E75°13′39′′H45.36.118.21.016.40.6S2
GRV020108S72°58′49′′ E75°15′20′′H45.81.418.51.016.51.6S1
GRV020109S72°58′49′′ E75°15′17′′H42.05.418.60.616.51.6S2
GRV020110S72°58′53′′ E75°14′59′′H43.17.318.71.516.61.1S2
GRV020113S72°58′48′′ E75°15′36′′H41.34.819.58.617.55.4S2
GRV020130S72°58′36′′ E75°15′37′′H4139.73.318.60.816.61.7S1
GRV021492S72°58′01′′ E75°16′24′′H4211.210.018.11.316.00.7S2
GRV021508S72°56′47′′ E75°17′00′′H4278.27.420.61.218.16.2S3
GRV021549S72°56′05′′ E75°19′18′′H416.31.517.61.417.43.2S2
GRV021550S72°56′05′′ E75°19′13′′H418.64.319.54.216.72.0S2
GRV021566S72°56′18′′ E75°17′23′′H413.50.819.02.217.32.6S2
GRV021569S72°56′25′′ E75°17′09′′H419.71.719.92.217.51.9S2
GRV021576S72°57′50′′ E75°12′58′′H4105.93.418.71.116.90.9S1
GRV021593S72°51′16′′ E75°12′39′′H428.16.019.11.616.91.8S4
GRV020023S73°05′09′′ E75°12′30′′H52.76.118.40.917.03.2S3
GRV020071S72°59′56′′ E75°12′15′′H54.52.718.21.716.60.8S2
GRV020076S72°59′43′′ E75°12′16′′H537.34.518.93.916.63.8S3
GRV020077S72°59′40′′ E75°12′18′′H51.33.220.03.617.62.3S3
GRV020087S73°00′08′′ E75°16′59′′H52.12.418.41.816.61.4S2
GRV020089S73°00′13′′ E75°15′05′′H54.68.518.71.316.91.1S2
GRV020092S72°59′45′′ E75°12′24′′H51.35.018.42.316.90.6S4
GRV020097S72°59′40′′ E75°12′15′′H5131.25.519.52.817.77.8S2
GRV020123S72°58′40′′ E75°15′36′′H53.46.219.21.217.21.3S1
GRV020153S72°58′50′′ E75°15′51′′H51.63.420.11.617.61.6S2
GRV020174S72°58′43′′ E75°15′37′′H51.33.719.91.517.63.4S3
GRV021480S72°56′07′′ E75°19′29′′H512.94.318.33.615.93.8S3
GRV021517S72°56′10′′ E75°18′49′′H596.44.018.91.317.02.0S2
GRV021518S72°56′11′′ E75°18′51′′H554.15.418.90.816.52.2S2
GRV021564S72°56′03′′ E75°19′20′′H513.75.018.43.616.32.7S2
GRV021589S72°57′57′′ E75°13′48′′H567.47.019.23.218.46.3S3
GRV021590S72°56′08′′ E75°17′54′′H516.53.919.21.216.82.3S3
GRV021611S72°46′31′′ E75°19′29′′H526.73.318.01.116.00.5S2
GRV021715S72°47′24′′ E75°17′47′′H51.51.217.43.915.41.9S4
GRV021795S72°46′26′′ E75°19′26′′H511.83.518.50.716.60.9S2
GRV020072S72°59′54′′ E75°11′45′′H613.03.720.61.918.55.2S3
GRV020093S72°59′44′′ E75°12′23′′H61.19.019.91.517.11.5S3
GRV020098S72°59′40′′ E75°12′16′′H6122.72.921.08.917.83.4S2
GRV021522S72°57′34′′ E75°14′13′′H61.26.617.31.715.62.5S4
GRV020038S73°08′37′′ E75°03′27′′L425.63.125.70.822.00.8S2
GRV020049S72°59′40′′ E75°12′34′′L41.24.225.12.121.21.4S2
GRV021643S72°46′22′′ E75°20′44′′L412.84.724.01.320.41.3S2
GRV021654S72°46′24′′ E75°19′55′′L416.63.025.61.821.92.9S3
GRV021668S72°46′43′′ E75°19′48′′L488.53.225.11.121.62.6S3
GRV021726S72°47′24′′ E75°17′22′′L411.24.025.31.221.53.0S3
GRV021800S72°46′24′′ E75°20′02′′L414.11.225.21.721.62.9S3
GRV022221S72°46′42′′ E75°19′15′′L429.13.325.00.921.11.5S4
GRV020040S73°08′05′′ E75°02′34′′L531.76.224.41.421.01.9S2
GRV020068S72°59′42′′ E75°12′21′′L5623.83.524.60.621.21.2S4
GRV020069S72°59′44′′ E75°12′28′′L5171.55.124.41.520.80.7S2
GRV020096S72°59′49′′ E75°12′22′′L51.80.924.74.920.220.2S3
GRV020107S72°58′48′′ E75°15′23′′L53.71.824.20.920.70.8S4
GRV020125S72°58′46′′ E75°15′37′′L52.13.924.90.621.41.1S4
GRV020127S72°58′50′′ E75°15′45′′L56.81.624.71.918.71.3S1
GRV020154S72°58′51′′ E75°15′40′′L51.52.926.62.922.01.0S2
GRV021495S72°56′48′′ E75°18′21′′L543.73.924.21.120.81.1S4
GRV021499S72°56′35′′ E75°17′48′′L557.13.923.10.719.70.7S2
GRV021500S72°56′57′′ E75°17′33′′L512.83.923.71.120.83.0S4
GRV021501S72°56′40′′ E75°17′55′′L517.42.524.01.520.70.8S3
GRV021548S72°57′46′′ E75°14′46′′L531.82.424.10.720.91.3S2
GRV021582S72°57′47′′ E75°13′28′′L514.25.324.22.720.51.3S4
GRV021586S72°57′43′′ E75°15′20′′L511.63.424.41.521.01.1S2
GRV021587S72°57′50′′ E75°13′31′′L531.33.724.22.720.51.0S2
GRV021614S72°46′24′′ E75°19′56′′L517.33.123.41.120.21.0S4
GRV021651S72°46′35′′ E75°20′52′′L535.24.124.60.721.10.8S3
GRV021652S72°46′28′′ E75°20′03′′L557.92.825.82.221.62.9S3
GRV021669S72°46′42′′ E75°19′49′′L5406.12.426.02.622.12.5S3
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GRV020115S72°58′43′′ E75°15′58′′L68.31.125.81.322.01.9S2
GRV020131S72°58′37′′ E75°15′40′′L63.83.926.04.121.81.1S2
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GRV022025S72°47′01′′ E75°17′47′′L6101.41.323.52.820.21.5S2
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GRV022130S72°46′44′′ E75°18′49′′L630.52.024.52.922.02.8S3
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GRV022132S72°46′44′′ E75°18′49′′L623.93.225.41.921.31.7S3
GRV022133S72°46′44′′ E75°18′49′′L621.43.225.20.421.31.3S3
GRV022134S72°46′44′′ E75°18′49′′L620.01.125.72.521.54.0S3
GRV022145S72°46′44′′ E75°18′49′′L631.83.323.51.019.90.9S2
GRV022147S72°46′44′′ E75°18′49′′L621.23.025.71.221.21.7S4
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GRV022149S72°46′44′′ E75°18′49′′L617.23.625.91.221.32.2S4
GRV022158S72°46′44′′ E75°18′49′′L614.21.523.62.020.64.4S4
GRV022162S72°46′54′′ E75°18′14′′L6141.01.824.11.720.71.0S3
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GRV022194S72°46′53′′ E75°18′20′′L615.62.825.83.321.33.8S5
GRV022220S72°46′42′′ E75°19′15′′L612.02.926.33.422.04.8S3
GRV022223S72°46′42′′ E75°19′15′′L671.23.125.71.721.43.4S3
GRV022237S72°46′43′′ E75°18′55′′L614.112.024.50.420.70.8S5
GRV022282S72°46′42′′ E75°18′50′′L643.33.324.11.320.61.5S2
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GRV022289S72°46′47′′ E75°17′34′′L638.12.124.14.922.13.7S4
GRV020021S73°05′11′′ E75°13′59′′LL411.32.227.53.423.74.2S1
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GRV020037S73°06′20′′ E75°10′14′′LL41.62.828.41.223.84.6S1
GRV020041S73°06′19′′ E75°09′08′′LL41.44.128.10.923.74.0S1
GRV020019S73°05′02′′ E75°12′59′′LL510.10.631.62.327.22.6S2

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Editorial for Special Issue “Nucleation of Minerals: Precursors, Intermediates and Their Use in Materials Chemistry”
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