ライフサイエンスコーパス: plagioclase

1 2-10 minutes, with pyroxenes, Fe-oxides, and plagioclase.

2 tz minerals including rutile, orthoclase and plagioclase.

3 nly by thermal conduction from hot vesicular plagioclase.

4 M of the PM10 was dominated by gypsum (36%), plagioclase (16%), Na sulphates (8%), and Fe-S-O phases

5 87)Sr/(86)Sr ratio yet measured on Earth, in plagioclase ((87)Sr/(86)Sr(initial) = 0.700050 +/- 0.000

6 mineral weathering of silicate rocks such as plagioclase, a calcium-sodium silicate do not match calc

7 ion of the fractionated leucogranites, while plagioclase accumulation results in enrichment of heavy

8 come first superheated and then saturated in plagioclase after stalling and cooling in shallow-level

9 oxene (Fs6Wo1), chromium diopside (Fs3Wo47), plagioclase (An14Or4), graphite, troilite, chromite, dau

10 x-ray diffraction (XRD) instrument revealed plagioclase (~An57), forsteritic olivine (~Fo62), augite

11 lute chemistry of the oxic water column with plagioclase and alumino-silicate weathering contributing

12 The data document that major minerals (plagioclase and biotite) commence to weather at 38 m dep

13 The boundary between amorphous plagioclase and crystalline high-pressure phases in our

14 standing the deformation of minerals such as plagioclase and for deriving constitutive models for the

15 sion-derived ash has an even distribution of plagioclase and glass, but boundaries enriched in pyroxe

16 T > 500 degrees C) isotopic exchange between plagioclase and nearly pristine meteoric fluid.

17 We find that carbonate, plagioclase and silica were melted and partly redistribu

18 nd 25% pigeonite), 40% sodic to intermediate plagioclase, and 15% olivine (forsterite 45% +/-5 to 10)

19 ts, containing normative olivine, pyroxenes, plagioclase, and accessory FeTi oxides.

20 wt % CaO) composed of olivine, Ti-magnetite, plagioclase, and clinopyroxene.

21 Olivine, plagioclase, and pyroxene demonstrate greater damage tha

22 ica glass (SiO2), fractured and shock-melted plagioclases, and spherulitic glass.

23 Plagioclase- and clinopyroxene-rich layers, hydrous pota

24 nvestigated the effects of 0.05 M sulfate on plagioclase (anorthite) dissolution and subsequent miner

25 (60-) (U(60)) to Na-montmorillonite (SWy-2), plagioclase (anorthite), and quartz (SiO(2)) as a functi

26 Plagioclase ( approximately 17 wt.% of bulk sample), tri

27 r replenishment by melts whose saturation in plagioclase as a single liquidus phase is triggered by t

28 fraction of glass and decreased fraction of plagioclase at particle boundaries, suggesting that frac

29 tions of diaplectic glass and maskelynite in plagioclase-bearing rocks are also suggested by the comb

30 issolution of formation rocks, which contain plagioclase, can affect the safety and efficiency of the

31 and several mafic subvolcanic orbicules and plagioclase comb layers from Northern California have di

32 sing these new constraints on disequilibrium plagioclase crystallization we also reproduce observed c

33 cts (>2 per mille) can occur during magmatic plagioclase crystallization.

34 ubidium/strontium, and europium anomaly) for plagioclase crystallization.

35 ata from 56 Thellier-Thellier experiments on plagioclase crystals separated from basalts of the Rajma

36 nt work on glassy melt inclusions trapped in plagioclase crystals to develop a method for tracking pr

37 tion transmission electron microscopy in two plagioclase crystals.

38 provide sufficiently accurate prediction of plagioclase dissolution at such high salinities.

39 r current understanding of cation effects on plagioclase dissolution does not provide sufficiently ac

40 findings can contribute to better predicting plagioclase dissolution in geologic formations and will

41 sites, where sulfate can potentially affect plagioclase dissolution/precipitation.

42 as a representative mineral of Ca-containing plagioclase) dissolution under conditions closely releva

43 thology along the traverse is basaltic, with plagioclase enrichment in stratigraphically higher locat

44 r and Sr/Y ratios, resulting from dominantly plagioclase extraction at slightly different pressures,

45 tope ratios measured from core to rim across plagioclase feldspar crystals can be used to monitor cha

46 chy-basaltic rocks with intergrown pyroxene, plagioclase feldspar, and altered olivine and overlying

47 imaging and analysis show that olivine and a plagioclase feldspar-rich mesostasis in the Lafayette me

48 s material and from regions composed of pure plagioclase feldspar.

49 n acquired its feldspar-rich crust by way of plagioclase flotation in a magma ocean.

50 Adcumulus growth of plagioclase from such melts at the chamber floor results

51 Heterogeneous oxygen isotope compositions of plagioclase from the Boehls Butte anorthosite include so

52 geneity (phosphorus in olivine and sodium in plagioclase) fundamentally inconsistent with prolonged r

53 New 40Ar/39Ar age determinations on plagioclase grains from deep boreholes in the basin reve

54 atios on agglutinates, volcanic glasses, and plagioclase grains from the Apollo sample collection.

55 n speciation, along with sulfur isotopes, in plagioclase-hosted melt inclusions and matrix glasses fr

56 We show that the volatile contents of plagioclase-hosted melt inclusions correspond to much hi

57 present a comparative study of olivine- and plagioclase-hosted melt inclusions from the Gakkel mid-o

58 of mantle melting increments represented by plagioclase-hosted melt inclusions, which were entrapped

59 d using electron backscatter diffraction, in plagioclase in andesite dome lavas from Volcan de Colima

60 epleted values (to -16 per mil) reported for plagioclase in meta-igneous rocks and indicate high-temp

61 rates that over 4.5 Ga of impact processing, plagioclase is on average weakly shocked (<15 GPa) and e

62 c Sr and Ca isotope measurements in magmatic plagioclase megacrysts from 3.7-2.8 Ga Archean anorthosi

63 te the corresponding magma crystallinity and plagioclase-melt geothermometry to determine the tempera

64 ppear to require parental melts saturated in plagioclase only but where and how to produce these melt

65 ficult to explain the calcic compositions of plagioclase overgrowth rims and microphenocrysts unless

66 The complex zoning patterns of plagioclase phenocrysts from 2003 to 2021 eruptions have

67 Plagioclase phenocrysts from the 1915 Mount Lassen rhyod

68 g trachy-andesitic lava with reversely zoned plagioclase phenocrysts in a K-rich groundmass.

69 Here we report melt inclusions trapped in plagioclase phenocrysts in andesite hosting the MtAp min

70 Our results show that plagioclase reaches equilibrium in 1-2 h, whereas ascent

71 lt that alters phase equilibria and triggers plagioclase resorption within regions that were initiall

72 Sr isotope heterogeneities in plagioclase reveal that multiple mush generations at Str

73 if-type anorthosites, enormous and enigmatic plagioclase-rich cumulate intrusions emplaced into Earth

74 g and modifying crystal cargoes by unlocking plagioclase-rich mushes and driving resorption, (re-)cry

75 d were compositionally less evolved than the plagioclase-rich rocks that followed.

76 esorption within regions that were initially plagioclase saturated.

77 A plagioclase separate from the Lagrange-1 exploration wel

78 Diaplectic glass and maskelynite in shocked plagioclase serve as key diagnostic features for high le

79 We observe weak correlations between plagioclase shock state and some REE+Y systematics (e.g.

80 ents are used to illustrate the viability of plagioclase sinking in iron-rich basaltic liquids and th

81 d rapidly from pressures (~0.7-2 GPa) at the plagioclase-spinel peridotite facies boundary to the sur

82 charges and mush remobilisations recorded by plagioclase suggest rapid magma-mush dynamics during vio

83 line with interlocking olivine-clinopyroxene-plagioclase textures and irregular shaped vesicles filli

84 Basaltic materials have more plagioclase than pyroxene, contain olivine, and are simi

85 the surface complexation between sulfate and plagioclase that can occur in GCS sites.

86 By focusing on a common mineral such as plagioclase, this approach can be applied across all maj

87 ts that a four to one mixture of pyroxene to plagioclase, together with about a 35 percent dust compo

88 To investigate how plagioclase trace-element systematics are affected by mo

89 dsorption of sulfate on anorthite, a Ca-rich plagioclase, was examined using attenuated total reflect

90 ow crystallisation ages are evaluated (e.g., plagioclase-whole rock Sm-Nd isochrons) and for what tra

91 mainly due to the lack of phase diagram for plagioclase with extended pressure-temperature condition