Myron G. Best. Igneous and metamorphic 2003 Blackwell Science

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APPENDIX A

Table A.1. Chemical Analyses of Representative Major Rock-Forming Minerals in Magmatic Rocks

LIVINE

ARNET

YROXENE

1 2 3 4 5 6 7 8 9 10 11 12 13

SiO

41.23 38.95 30.25 41.55 58.13 52.52 51.52 55.08 51.5 41.5 48.48 51.92 54.76

TiO

0.02 0.04 0.11 0.04 0.71 0.18 0.07 1.2 4.8 0.08 0.77 0.44

0.03 0.02 0.00 20 28 0.79 1.10 0.32 2.24 2.2 10.4 0.3 1.85 8.33

0.02 0.02 4.8 0.33 0.06 2.03 0.0 0.0

4.3 7.4 31.44 1.29

FeO 7.50t 18.16t 61.88t 6.93t 4.53t 18.0t 26.96t 2.21t 5.2 1.7 26.97t 0.75 2.70

NiO 0.45 0.01 0.01 0.11 0

MnO 0.08 0.20 6.14 0.37 0.12 0.33 2.06 0.09 0.0 0.1 2.57 0.04

MgO 50.76 42.37 1.40 20.88 35.39 25.1 17.69 16.40 15.4 10.6 2.46 11.59

CaO 0.02 0.32 0.19 5.04 0.46 2.15 1.30 19.65 19.6 22.8 18.16 16.35

O 0.03 0.02 0.03 0.13 0.03 0.05 0.4 0.9 0.59 12.86 4.63

O 0.00 0.00 0.00 0.00 0.01 0.1 0.1 0.19 0.05

Total 100.15 100.11 99.86 100.10 100.01 100.00 100.03 99.88 99.9 100.3 99.61 99.78 100.18

1, Mg-rich olivine (Fo

92.3

) in coarse garnet lherzolite xenolith in kimberlite, Bulfontein, Kimberly, South Africa. From same rock as analyses 4, 5, and 8.

(Data and chemical and modal compositions of the whole rock from Cox et al., 1987.) 2, Mg-rich olivine (Fo

80.6

), rim of phenocryst in basalt scoria, 1959

eruption of Kilauea volcano, Hawaii. (From Helz, 1987.) 3, Fayalite (Fo

3.5

) phenocryst in rhyolitic Bandelier Tuff, Valles caldera complex, New Mexico.

From same rock as analyses 7 and 11. (Data from Warshaw and Smith, 1988.) 4, Pyropic garnet in coarse garnet lherzolite xenolith in kimberlite, Bul-

fontein, Kimberly, South Africa. From same rock as analyses 1, 5, and 8. (Data and chemical and modal compositions of the whole rock from Cox et al.,

1987.) 5, Enstatite (Fn

93.2

) in coarse garnet lherzolite xenolith in kimberlite, Bulfontein, Kimberly, South Africa. From same rock as analyses 1, 4, and

8. (Data and chemical and modal compositions of the whole rock from Cox et al., 1987.) 6, Hypersthene (En

68.3

) in groundmass in the prehistoric

Makaopuhi lava lake, Kilauea volcano, Hawaii. (Data from Evans and Moore, 1968.) 7, Hypersthene (En

52.1

) phenocryst in rhyolitic Bandelier Tuff,

Valles caldera complex, New Mexico. From same rock as analyses 3 and 11. (Data from Warshaw and Smith, 1988.) 8, Cr-rich diopside in coarse garnet

lherzolite xenolith in kimberlite, Bulfontein, Kimberly, South Africa. From same rock as analyses 1, 4, and 5. (Data and chemical and modal composi-

tions of the whole rock from Cox et al., 1987.) 9, Augite groundmass grain in tholeiitic basalt, Santa Clara lava ﬂow, Saint George, Utah. (Data from Best

and Brimhall, 1974.) 10, Ti-rich augite groundmass grain in basanite lava, Uinkaret plateau, northwestern Grand Canyon, Arizona. (Data from Best and

Brimhall, 1974.) 11, Fe-rich augite phenocryst in rhyolitic Bandelier Tuff, Valles caldera complex, New Mexico. From same rock as analyses 3 and 7. (Data from

Warshaw and Smith, 1988.) 12, Aegirine in peralkaline A-type granite, south Kigom Hills, Nigeria. From same rock as analysis 17. (Data from

Greenwood, 1951.) 13, Omphacite in eclogite xenolith, Kao kimberlite pipe, Basutoland, South Africa. (Data from Nixon et al., 1963.)

658 Igneous and Metamorphic Petrology

Table A.1. (Continued)

MPHIBOLE

ICA

14 15 16 17 18 19 20 21

SiO

44.48 44.6 40.96 51.01 55.4 48.51 35.93 40.62

TiO

1.69 1.2 3.92 0.96 0.46 1.10 4.27 2.27

7.47 13.4 15.35 0.80 0.99 1.08 13.00 11.26

2.7 0.27 0.48

3.91 4.82 16.41 17.53 2.61

FeO 17.70 3.4t 3.30 17.62 2.25t 14.31 20.81 5.42t

MnO 0.26 0.05 0.48 0.66 0.11 0.06

MgO 9.34 18.1 15.24 0 22 22.9 1.31 9.26 24.67

CaO 10.72 10.1 10.42 0.19 6.74 5.43 0.41 0.13

O 1.46 3.4 2.56 7.98 3.82 7.87 0.10

O 0.97 1.3 1.74 1.80 4.63 1.48 10.14 10.13



1.47 1.00 0.91 1.48 2.69 3.09

F 0.31 0.02 1.70 0.65

Cl 0.12

Total 99.78 98.2 99.77 100.09 97.67 100.76 99.98 98.94

14, Hornblende in quartz monzodiorite, Gaudalupe igneous complex, California. From same rock as analysis 20. (Data from Best and Mercy, 1967.)

15, Cr-rich pargasite as interstitial grains in spinel lherzolite xenolith in basanite, Uinkaret plateau, Arizona. (Data from Best, 1974.) 16, Kaersutite iso-

lated anhedral megacryst in basanite, Uinkaret plateau, Arizona. (Data from Best, 1974.) 17, Riebeckite in peralkaline A-type granite, south Kigom Hills,

Nigeria. From same rock as analysis 12. (Data from Greenwood, 1951.) 18, Richterite; mean of 27 in veined metasomatized garnet peridotite xenoliths,

Bultfontein, South Africa. (Data from Dawson, 1987.) 19, Arfvedsonite in A-type syenite, Morotu, Sakhalin Island, Russia (north of Japan). (Data from

Yagi, 1953.) 20, Biotite in quartz monzodiorite, Gaudalupe igneous complex, California. From same rock as analysis 14. (Data from Best and Mercy,

1967.) 21, Phlogopite in mica-rich minette lamprophyre dike, Wasatch plateau. Utah. Analysis of whole rock in Table 13.11, column 6. (Data from Tingey

DG, unpublished MS thesis, Brigham Young University, Provo, Utah, 1989.)

ELDSPAR

ELDSPATHOID AND

ELDSPATHOID

-T

XIDE

22 23 24 25 26 27 28 29 30 31 32

SiO

67.84 62.7 52.42 44.17 65.5 44.35 54.62 47.23 42.81 0.07 0.03

TiO

0.00 0.09 0.00 0.12 3.9 48.6

19.65 23.27 29.7 34.95 19.03 32.22 22.93 26.72 6.59 2.7 0.07

1.0 0.05

0.08 0.05

0.03 0.19t 0.36 0.56 0.09t 0.47t 0 26 1.29t 1.90 58.1 8.8

FeO 0.02 0.13 0.08 0 26 3.06 34.0 39.8

MnO 0.08 0.28 0.44

MgO 0.04 0.08 0.00 0.23 0.00 7.48 0.7 1.9

BaO 0.02 0.16

CaO 0.00 4.35 12.65 18.63 0.18 0.54 0.08 1.40 33.27 0.03 0.04

O 11.07 8.58 4.01 0.79 3.84 19.69 0.66 14.70 3.75

O 0.29 1.23 0 21 0.05 11.19 1.93 21.02 0.73 0.33



0.56 0.84 0.53 0.12 8.23 0.43

Total 99.50 100.34 99.65 100.07 99.99 99.96 99.95 100.30 99.82 99.87 99.78

22, Albite in pegmatite, near Court House, Amelia County, Virginia. An

0.3

, Ab

98.0

, Or

1.7

. (Data from Kracek and Neuvonen, 1952.) 23, Oligoclase in

rhyolitic Bishop Tuff, California. An

20.4

, Ab

72.7

, Or

6.9

. From same rock as analysis 26. (Data from Hildreth W, unpublished Ph.D thesis, University of

California, Berkeley, 1977.) 24, Labradorite isolated megacrysts in basaltic scoria, Crater Elegante, Sonora, Mexico. An

63.1

, Ab

35.7

, Or

1.2

. (Data from

Gutman and Martin, 1976.) 25, Anorthite in olivine norite, Grass Valley, California. An

92.6

, Ab

7.1

, Or

0.3

. (Data from Kracek and Neuvonen, 1952.)

26, Sanidine in rhyolitic Bishop Tuff, California. An

0.9

, Ab

33.9

, Or

65.0

. From same rock as analysis 23. (Data from Hildreth W, unpublished Ph.D thesis,

University of California, Berkeley, 1977.) 27, Nepheline in theralite (olivine-nepheline-analcite gabbro), Square Top intrusion, New South Wales, Aus-

tralia. From same rock as analysis 29. (Data from Wilkinson, 1965.) 28, Leucite in leucitite, Lake Kivu National Park, Zaire. (Data from Sahama, 1952.)

29, Analcite in theralite (olivine-nepheline-analcite gabbro), Square Top intrusion, New South Wales, Australia. From same rock as analysis 27. (Anal-

cite is actually a zeolite but occurs in some rocks as if it were a feldspathoid.) (Data from Wilkinson, 1966.) 30, Melilite in melilite nephelinite, Honolulu,

Oahu, Hawaii. Whole rock analysis in Table 13.2, column 7. (Melilite is not a feldspathoid, but its occurrence in some rocks is like that type of mineral.

(Data from Neuvonen, 1952.) 31, Magnetite in groundmass in the prehistoric Makaopuhi lava lake, Kilauea volcano, Hawaii. From same rock as analy-

sis 32. (Data from Evans and Moore, 1968.) 32, Ilmenite in groundmass in the prehistoric Makaopuhi lava lake, Kilauea volcano, Hawaii. From same

rock as analysis 31. (Data from Evans and Moore, 1968.)

Appendix A

659

Table A.2. Chemical Analyses of Representative Major Rock-Forming Minerals in Metamorphic Rocks

HYLLOSILICATES

EOLITES

LAY MINERALS

ICAS

12 3456 78 9101112

SiO

50.63 56.8 46.60 51.14 52.87 27.54 50.24 46.17 44.41 44.89 35.98 43.70

TiO

0.0 0.00 0.00 1.02 0.09 0.27 1.07 0.22 0.15 0.00 trace

22.07 16.60 39.52 19.76 24.91 18.96 25.72 33.85 40.09 6.98 3.19 24.05

trace 0.09 0.83 0.78 1.22 0.27 0.99 1.72 28.80 6.36 0.93

FeO 0.00 1.19 24.36 3.07 0.99 0.28 1.02 1.72 0.03

MnO 0.43 0.01 trace 0.02 2.74 0.09 0.00

MgO 0.40 trace 0.15 3.22 3.60 15.62 3.69 1.44 0.16 5.23 37.6 0.11

CaO 10.72 5.8 0.23 1.62 0.69 0.08 0.00 0.00 0.67 0.65 0.00 26.85

O 1.08 1.6 0.09 0.04 0.22 0.14 0.45 1.08 5.80 0.42 0.00 0.04

O 0.45 0.8 0.01 0.11 7.98 0.08 10.39 9.60 2.22 1.30 0.00 0.00



14.10 12.45 13.90 7.99 6.73 11.20 4.44 4.52 4.45 6.59 14.16 4.54



3.3 14.81 2.56 0.06 0.02 0.07 1.58 0.03

Total 99.45 99.35 100.39 99.75 99.61 99.78 100.02 99.75 100.04 100.35 100.27 100.28

1, Laumontite, vitric tuff, Otama, New Zealand (Coombs, 1952). Total water 14.10 wt.%. 2, Heulandite, Cape Blomidon, Nova Scotia. In-

cludes 2.0 wt.% SrO (Coombs et al., 1959). 3, Kaolinite, Keokuk, Iowa (Newman and Brown, 1987). 4, Montmorillonite (smectite), Mont-

morillon, France (Ross and Hendricks, 1945). 5, Illite, Burnt Bluff Group, Fond du Lac County, Wisconsin (Hower and Mowatt, 1966). 6,

Chlorite in blue-schist tectonic block several meters in diameter encased in serpentinite, Franciscan Complex, Cazadero, California (Lee et al.,

1966). From same rock as phengite (analysis 7), glaucophane (18), pumpellyite (13), and epidote (14). 7, Phengite in blue-schist tectonic block

several meters in diameter encased in serpentinite, Franciscan Complex, Cazadero, California (Lee et al., 1966). Includes 1.45 wt.% BaO. From

same rock as chlorite (analysis 6), glaucophane (18), pumpellyite (13), and epidote (14). 8, Muscovite in biotite–plagioclase–epidote–

quartz–garnet schist, Morar, Inverness-shire, Scotland (Lambert, 1959). 9, Paragonite in muscovite–quartz–chlorite–Fe–Ti oxide schist, Glebe

Mountain, southern Vermont (Rosenfeld, 1956). 10, Stilpnomelane in quartz–albite–glaucophane schist, Franciscan Complex, San Juan

Bautista Mine, Santa Clara County, California (Hutton, 1956). 11, Serpentine (chrysotile and lesser lizardite) in serpentinized lherzolite in ophi-

olite, New Almaden Mine, Santa Clara County, California (Faust and Fahey, 1962). Includes 0.04 wt.% S, 0.29 Cr

, and 0.84 CO

. Total wa-

ter is 14.16 wt.%. 12, Prehnite in cavities in altered diabase, Prospect Quarry, New South Wales, Australia (Coombs et al., 1959).

Table A.2. (Continued)

MPHIBOLES

ARNETS

13 14 15 16 17 18 19 20 21 22 23 24

SiO

37.48 38.11 59.45 54.73 50.88 55.04 57.79 27.36 47.69 36.56 39.30 38.14

TiO

0.20 0.50 0.21 1.86 0.22 0.91 0.73 trace 0.51 0.00 0.29

25.43 25.75 0.49 1.46 8.53 9.06 21.41 52.12 32.52 21.07 21.93 30.91

1.29 9.66 0.00 0.00 4.25 2.83 3.39 1.11 0.63 0.47 0.80 1.56

FeO 3.16 0.64 0.07 9.60 13.41 11.62 0.65 13.09 8.04 33.51 0.28 0.13

MnO 0.83 0.10 0.38 0.16 0.23 0.04 0.10 0.04 1.81 0.01

MgO 2.94 0.14 25.19 17.94 8.50 9.64 0.75 2.44 7.56 3.97 trace 0.03

CaO 22.14 23.41 11.88 12.76 5.19 3.58 1.16 0.29 0.52 1.61 37.10 17.54

O 0.32 0.00 1.44 4.63 5.50 12.99 0.10 0.53 0.06

O 0.02 0.00 trace 0.03 0.05 0.32 0.34 0.42 0.14



6.36 1.78 2.27 2.27 2.44 1.99 0.18 2.47 1.85 0.30 10.72



0.02 0.00 0.00 0.00 0.00 0.00 0.14 0.55

Total 100.19 100.09 99.73 100.57 99.95 99.53 99.73 100.05 100.35 99.51 99.84 99.53

13, Pumpellyite in blue-schist tectonic block several meters in diameter encased in serpentinite, Franciscan Complex, Cazadero, California (Lee

et al., 1966). From same rock as chlorite (analysis 6), phengite (7), glaucophane (18), and epidote (14). 14, Epidote in blue-schist tectonic block

several meters in diameter encased in serpentinite, Franciscan Complex, Cazadero, California (Lee et al., 1966). From same rock as chlorite

(analysis 6), phengite (7), glaucophane (18), and pumpellyite (13). 15, Tremolite in calcite-bearing skarn, Adirondack Mountains, Balmat,

New York (Weeks, 1956). 16, Actinolite in albite-clinozoisite-bearing schist, Limebury Point, Salcombe Estuary, South Devon, England

(Tilley, 1938). 17, Crossite in hornblende-epidote-titanite-albite amphibolite, Ayrshire, Scotland (Bloxam and Allen, 1960). 18, Glaucophane

in blue-schist tectonic block several meters in diameter encased in serpentinite, Franciscan Complex, Cazadero, California (Lee et al., 1966).

From same rock as chlorite (analysis 6), phengite (7), pumpellyite (13), and epidote (14). 19, Jadeite in blueschist-facies metagraywacke of the

Franciscan Complex, Pacheco Pass (about 130 km southeast of San Francisco), California (Ernst et al., 1970). See Figure 18.29. 20, Staurolite

in quartz–biotite–muscovite–garnet schist, about 0.2 km west of Rinvyle Church, County Galway, Ireland (Leake, 1958). 21, Cordierite in

garnet–spinel–plagioclase–biotite hornfels, Sparcraigs, Belhelvie, Aberdeenshire, Scotland (Stewart, 1942). Same rock as almandiferous garnet

(analysis 22). 22, Almandiferous garnet in spinel–cordierite–plagioclase–biotite hornfels, Sparcraigs, Belhelvie, Aberdeenshire, Scotland (Stew-

art, 1942). Same rock as cordierite (analysis 21). 23, Grossular with vesuvianite in rodingite veins in serpentinite, Georgetown, California

(Pabst, 1936). 24, Lawsonite with pumpellyite in glaucophane schist tectonic block hosted in serpentinite, Berkeley Hills, California (Davis and

Pabst, 1960).

660 Igneous and Metamorphic Petrology

Calculation of the CIPW Norm

In this normative calculation, devised by W. Cross,

J. P. Iddings, L. V. Pirsson, and H. S. Washington,

constituents from the chemical analysis of a rock are

allocated in a prescribed sequence to hypothetical nor-

mative minerals. These have simple end-member com-

positions and all are volatile-free.

The normative minerals and their abbreviations,

chemical formulas, and formula weights are shown in

Table B.1. Examples of the calculation are shown in

Tables B.2 and B.3. During the calculation, numbers

should be rounded to four signiﬁcant digits.

The oxidation state of Fe in the chemically analyzed

rock can profoundly affect the degree of silica satura-

tion in the norm. Because this degree of silica satura-

tion is one of the primary reasons for making the

calculation, the oxidation state must be standardized in

some way. This is particularly important for hot extru-

sive rocks that oxidized in the oxygen-rich atmosphere

or hydrosphere. Cox et al. (1979) suggest using a stan-

dard molecular ratio of Fe

/FeO  0.15, which is

equivalent to an atomic ratio of Fe

3

/Fe

2

 0.30. The

3

/Fe

2

ratio of the low-K basaltic andesite in Table

13.6, whose norm is calculated in Table B.2, is stan-

dardized as follows:

.% F

ORMULA

TOMIC

OTAL

XIDE

. O

XIDE

ROPORTION

** P

ROPORTION

TOMS

3.47 159.69 0.0217 0.0434

0.1524

FeO 7.83 71.846 0.1090 0.1090

* Sum of atomic weights.

** Wt.% oxide divided by formula wt. of oxide.

Simultaneous solution of the two equations in atomic

amounts

3

/Fe

2

 0.30

3

 Fe

2

 0.1524

gives Fe

2

 0.1172 and Fe

3

 0.0352. As a check,

3

/Fe

2

 0.3003.

The standardized formula proportion of FeO 

0.1172 and of Fe

 0.0352/2  0.0176. These two

proportions are used in the calculation in Table B.2.

The following calculation procedure ignores several

constituents seldom found in analyses of common

rocks. If the analysis includes NiO, add its formula

proportion to FeO, add SrO and BaO to CaO, allocate

F to Ap (3P

 0.33F), and if in excess, to make

normative ﬂuorite after step 5, Cl is allocated to nor-

mative halite after step 2, ZrO to normative zircon, and

Cr (and FeO) to normative chromite before making

normative ilmenite and magnetite.

1. Calculate the formula (molecular) proportions

of the oxides in the chemical analysis by dividing

their weight percentage (wt.%) by their corre-

sponding formula weight, as was done for Fe

and FeO.

2. Add the proportion of MnO to that of FeO.

3. Allocate an amount from the formula proportion of

CaO equal to 3.3 times that of the formula propor-

tion of P

to make normative apatite (Ap).

4. Allocate an amount of FeO equal to that of the pro-

portion of TiO

to make normative ilmenite (Il ).

5. If there is an excess of TiO

over available FeO,

allocate an amount of CaO equal to the excess to

APPENDIX B

Table B.1. Data for normative minerals

HEMICAL

ORMULA

AME

BBREVIATION

ORMULA

EIGHT

Quartz Q SiO

60.08

Corundum C Al

102.0

Orthoclase Or K

O · Al

· 6SiO

556.6

Albite Ab Na

O · Al

· 6SiO

524.4

Anorthite An Ca

O · Al

· 2SiO

278.2

Leucite Lc K

O · Al

· 4SiO

436.5

Nepheline Ne Na

O · Al

· 2SiO

284.1

Kaliophilite Kp K

O · Al

· 2SiO

316.3

Acmite Ac Na

O · Fe

· 4SiO

462.0

Sodium Ns Na

O · SiO

122.1

metasilicate

Potassium Ks K

O · SiO

154.3

metasilicate

Wollastonite Wo CaO · SiO

116.2

Diopside Di CaO · FeO · 2SiO

248.1

CaO · MgO · 2SiO

216.5

Hypersthene Hy FeO · SiO

131.9

MgO · SiO

100.4

Olivine Ol 2FeO · SiO

203.8

2MgO · SiO

140.7

Dicalcium Cs 2CaO · SiO

172.2

silicate

Magnetite Mt FeO · Fe

231.5

Ilmenite Il FeO · TiO

151.7

Hematite Hm Fe

159.7

Titanite Tn CaO · TiO

· SiO

196.0

Perovskite Pf CaO · TiO

135.9

Rutile Ru TiO

79.87

Apatite Ap 3.3 CaO · P

327.0

Table B.2. Calculation of the Normative Composition of the Low-K Basaltic Andesite in Table 13.6

.% F

ORMULA

XIDE

EIGHT

ROPORTION

Ap Il Or Ab An Mt Rem Di Hy Q

SiO

53.29 60.08 0.8870 0.0192 0.2136 0.2582 0.0912 0.1625 0.1423

TiO

0.91 79.87 0.0114 0.0114

17.13 102.0 0.1679 0.0032 0.0356 0.1291

3.47 159.7 0.0176

0.0176

FeO 7.83 71.85 0.1172

0.0114 0.0176 0.0910 0.0199 0.0711

MnO 0.20 70.94 0.0028

MgO 4.72 40.30 0.1171 0.1171 0.0257 0.0914

CaO 9.87 56.08 0.1760 0.0013 0.1291 0.0456 0.0456

O 2.21 62.00 0.0356 0.0356

O 0.30 94.20 0.0032 0.0032

0.06 141.9 0.0004 0.0004

Wt.% normative mineral 0.13 1.73 1.78 18.67 35.92 4.07 10.50 18.56 8.55

* Proportions adjusted so that the molecular Fe

/FeO ratio  0.15. FeO/MgO  0.7771 in Rem.

Table B.3. Calculation of the Normative Composition of the Orangeite in Table 13.11

.% F

ORMULA

XIDE

EIGHT

ROPORTION

Ap Il Or Ks Ac Mt Rem Di Hy Ol Lc Or

SiO

35.09 60.08 0.5841 0.1500 0.0059 0.0116 0.0928 0.7269 0.3631 0.0784 0.0324

TiO

1.06 79.87 0.0133 0.0133

2.55 102.0 0.0250 0.0250 0.0196 0.0054

7.78t 159.7 0.0113* 0.0029 0.0113

FeO 71.85 0.0749* 0.0133 0.0113 0.0524 0.0032 0.0492 0.0493

MnO 0.15 70.94 0.0021

MgO 29.02 40.3 0.7201 0.7201 0.0432 0.6769 0.6768

CaO 3.49 56.08 0.0622 0.0158 0.0464 0.0464

O 0.18 62.00 0.0029 0.0029

O 2.91 94.20 0.0309 0.0250 0.0059 0.0196 0.0054

0.68 141.9 0.0048 0.0048

Wt.% normative mineral (Step. 30.) 1.57 2.02 0 0.91 1.34 2.62 10.14 0 52.63 8.56 3.01

Step 22. D  0.4023

23. D  Hy/2  0.7261/2  0.3631; Ol0.3631; Hy  0; D

 0.4023  0.3631  0.0392

24. D

 D

 0.0392

25. D

 4Ab0; Ne  Ab0; D

 D

 4Ab0.0392

26. D

 2Or0.0500; Lc  D

/2  0.0392/2  0.0196; OrD

/2  0.0250  0.0196  0.0054

* Proportions adjusted so that the molecular Fe

/FeO ratio  0.15. FeO/MgO  0.0728 in Rem.

664 Igneous and Metamorphic Petrology

make provisional titanite (Tn), but only after the

allocation of CaO to make normative anorthite

(step 12).

6. If there is still an excess of TiO

over available

CaO, this latter excess is used to make normative

rutile (Ru).

7. Allocate an amount of Al

equal to the propor-

tion of K

O to make provisional normative ortho-

clase (Or).

8. If there is an excess of the proportion of K

O over

that of Al

, this excess is made into normative

potassium metasilicate (Ks). The rock is peralka-

line.

9. From any excess of Al

in step 5, an equal

amount is allocated to the proportion of Na

O to

make provisional normative albite (Ab).

10. If there is an excess of Na

O, it is allocated, to-

gether with an equal amount of Fe

, to make

normative acmite (Ac). The rock is peralkaline.

11. If there is still an excess of Na

O from step 10, it is

made into normative sodium metasilicate (Ns). The

rock is peralkaline.

12. If there is an excess of Al

over that used to

make provisional normative Or and Ab in steps 7

and 9, this excess is allocated to an equal amount of

CaO to make normative anorthite (An).

13. If there is an excess of Al

over that required for

An in step 12, it is made into normative corundum

(C). The rock is peraluminous.

14. To the proportion of Fe

(or the excess of Fe

over that used in making Ac in step 10) an equal

amount of FeO is allocated for normative mag-

netite (Mt).

15. If there is an excess of Fe

over that required for

Mt in step 14 it is made into normative hematite

(Hm).

16. All of the FeO and CaO remaining from the previ-

ous allocations, together with the proportion of

MgO, are entered into a remainder column (Rem).

Calculate the FeO/MgO ratio.

17. Allocate to the remaining CaO an equal amount of

(FeO  MgO) to make provisional normative diop-

side (Di); the relative amounts of FeO and MgO al-

located must be in the ratio in which they occur in

the Rem column.

18. If there is an excess of CaO required to make Di in

step 17, this excess is made into provisional norma-

tive wollastonite (Wo).

19. If there is an excess of (FeO  MgO) required to

make Di in step 17, this excess is made into provi-

sional normative hypersthene (Hy). The relative

amounts of FeO and MgO so allocated should be

in the same ratio as in the Rem column.

All of the oxides except SiO

have now been

allocated to actual or provisional normative minerals.

In the next steps, SiO

is distributed to silicate norma-

tive minerals. If there is an excess in this distribution,

the rock is silica-oversaturated. If there is a deﬁciency

of SiO

, the rock is silica-undersaturated, and adjust-

ments must be made in the amounts of one or more

provisional normative minerals so that there is sufﬁ-

cient SiO

to go around.

20. Allocate the necessary amounts of SiO

to the sili-

cate minerals. For example, allocate six times the

amount of K

O for Or, an equal amount to that of

CaO  FeO  MgO for Di, and so forth. Let this

necessary amount of SiO

be Y.

21. If Y is less than the available formula proportion of

SiO

calculated in step 1, the excess is made into

normative quartz (Q). Go to step 30.

22. If Y is greater than the available SiO

, the deﬁ-

ciency must be compensated for by reducing the

amounts of silica-saturated provisional normative

minerals (feldspars, pyroxenes) and creating new

silica-unsaturated normative minerals (feldspa-

thoids, olivine). Set the deﬁciency, D, equal to Y

minus available SiO

23. If D  Hy/2 make normative olivine Ol  D and

make normative hypersthene Hy  Hy2D. The

relative amounts of FeO and MgO in Ol and Hy

should be in the same ratio in which they occur in

the Rem column. The deﬁciency in SiO

should

now be zero. If D  Hy/2, make provisional nor-

mative olivine OlHy/2 and Hy  0. Let D



D  Hy/2.

24. If no Tn was made in step 5, let D

 D

and go to

step 25. If Tn was made in step 5 and D

 Tn/2,

make normative titanite, Tn  Tn D

, and make

normative perovskite, Pf  D

. The deﬁciency

in SiO

should now be zero. If D

 Tn/2, make

normative perovskite, Pf  Tn and Tn  0. Let

 D

25. If D

 4Ab, let normative nepheline Ne  D

and normative albite Ab  Ab D

/4. The deﬁ-

ciency in SiO

should now be zero. If D

 4Ab,

let Ne  Ab and Ab  0. Let D

 D

 4Ab.

26. If D

 2Or, let normative leucite, Lc  D

/2,

and normative orthoclase, Or  Or D

/2.

The deﬁciency in SiO

should now be zero. If

 2Or, let Lc  Or and Or  0. Let D



 2Or .

27. If no Wo was made in step 18, let D

 D

and go

to step 28. If Wo was made in step 18 and D



Wo/2, let normative dicalcium silicate Cs  D

and normative wollastonite Wo  Wo 2D

The deﬁciency in SiO

should now be zero.

If D

 Wo/2, let Cs Wo/2 and Wo  0. Let

 D

 Wo/2.

28. If D

 Di, add an amount equal to D

/2 to

the amounts of Cs and Ol already determined

in steps 27 and 23, respectively. Let Di  Di D

The deﬁciency in SiO

should now be zero. If

 Di, add an amount equal to Di/2 to the

amounts of Cs and Ol already determined in steps

27 and 23, respectively. Let Di  0 and D



 Di.

29. Let normative kaliophilite Kp  D

/2 and Lc 

Lc D

/2. The deﬁciency in SiO

should now be

zero.

30. All of the normative amounts are converted into the

weight percentage (wt.%) by multiplying them by

the formula weights of the normative minerals in

Table B.1. For example, the weight percentage of

Or in the low-K basaltic andesite in Table B.2 is

0.0032  556.6  1.78; the weight percentage of Di

is (0.0257  216.5)  (0.0199  248.1)  5.56 

4.94  10.50. The ﬁnal weight percentages of nor-

mative minerals are rounded to three signiﬁcant dig-

its. Rounding in the calculations may cause the nor-

mative total to differ somewhat from the oxide total.

Appendix B

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