Table 1 Summary of experimental results

From: Melting at the base of a terrestrial magma ocean controlled by oxygen fugacity

Exp.

Starting comp.

T (°C)

P (GPa)

Duration (h)

log fO2

Glass proportion (wt%)

Mineral proportions (wt%)

New solidus (°C) at high fO2

Ave. \(\Delta\)T (°C)

Gt

Wd

Rw

Bg

Fp

Cpv

H5340

 

1,600

16

6

IW + 2.0 ± 0.1 (MH)

0

53

47

    

1,680

 

H5364

 

1,700

 

3

 

2

54

44

      

S7620

 

1,800

 

2

 

14

44

42

      

H5452

 

1,800

21

3

 

0

54

 

46

   

1,900

340 ± 110

H5336

Pyrolite

1,900

 

2

 

1

64

 

31

 

4

   

H5323

 

2,000

 

2

 

80

20

       

I-1108

 

1,700

26

12

 

0

   

81

11

8

2,050

 

I-1107

 

1,900

 

3

 

0

   

80

12

8

  

I-1137

 

2,000

 

2

 

0

   

82

12

6

  

I-1095

 

2,100

 

0.5

 

3

   

89

1

7

  

L-1

Pyrolite + Ir

1,900

26

2

IW + 2.0 ± 0.1 (MH)

0

   

79

13

8

  

L-2

 

2,200

 

2

IW − 1.2 ± 0.2 (Re capsule)

0

   

80

13

7

  
  1. T, temperature; P, pressure; Exp., experiment; comp., composition; phase proportion calculated using least squares mass balance and compositions from electron microprobe analysis (EMPA) in wt% oxides. Mineral abbreviations: Gt, garnet; Wd, wadsleyite; Rw, ringwoodite; Bg, bridgmanite; Fp, ferropericlase; Cpv, CaSiO3-rich perovskite; Ir, iridium. The solidus at 16 and 21 GPa is obtained by a straight line fit of experimental temperature versus melt percentage; the error bar for our new solidus at each pressure is ≤50 °C; Ave. ΔT is the difference in solidus temperature due to a ~ 3.2 log units average difference in fO2 (MH powder versus Re capsule control).
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