THn AUERTcAN MTUERALocIST
JOURNAL OF THE MINERALOGICAL

Vol. 35

SOCIETY OF AMERICAJANUARY.FEBRUARY, 1950

TIJE L AZULITE-SC ORZ ALITEISOMORPHOUS

Nos. I and 2

SERIESI

W. T. PncoRA ANDJ. J. F,o.nrv, U. S. GeologicalSuruey,
Washington,D. C.
CoNtrNrs
lntroduction..
Sample selection and separation
Description of selected specimens
Descriptlve mineralogy
Morphology
Variation in chemical composition.
Invalidity of calcium lazulite
Series nomenclature.
Variation in specific gravity.
Variation in optical properties.
X-ray data.
Occurrence. . .
General association. . ..
Occurrence in quartzite
Occurrence in quartz-rich veins and dikes.
Occurrence in granitic pegmatites.
Occurrence in alluvium and colluvium.
Gem lazulite
Acknowledgments. . .
References

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Assrnecr
The lazulite-scorzahte isomorphous series-expressed by the oxide formula (Mg,established in this paper on the basis of chemical analyses,
Fe")O'AlzO:'PzOs'HzO-is
indices of refraction, and specific gravity of eight selected specimens. The data for sixof these are new. The molecular ratio of Mg:Fe in these analyses ranges from 88:12 to
24:76, with the weight per cent of MgO ranging from 11 97 to 2 93, and.the weight per centof FeO correspondingly from 2.80 to 17.06. The progressive increase in divalent iron iscorrelated with a progressive increase of indices of refraction, specific gravity, and birefringence. Evidence is submitted that discredits the name calcium Iazulite; for tbe significant percentages of CaO and of SiO2, reported in more than two dozen analvses in the literature are believed to be the result of chemical analyses of impure samples. Geologicaloccurrences of lazulite and scorzalite are classifed into four groups and world-wide geographic occurrences are noted in accordance with this classification.
I Published by permission of the Director, U. S. Geological Survey.

W. T. PECORA AND T. J. FAHEY

INrnooucrroN
The lazulite-scorzalite isomorphous series-expressed by the oxide
formula (Mg, Fe")O.AlzOa.PzOr.HzO-is establishedessentiallyfrom
the data obtained by the writers on 8 selectedsamples representative of
the series. The name lazulite has been used for over a century but thename scorzalite was only recently introduced by Pecora and Fahey(1949a) for the iron analogue of lazulite.
Most of the forty or so chemical analyses of lazulite available in theliterature are not acceptable for use in this series because three rigid
requirements so necessaryin preparing a variation diagram were not fulfilled: (1) reliable chemical analysis on samples plus-99 per cent pure;(2) specific gravity determined on a portion of the analyzed sample; and(3) precise optical data determined on a split of the analyzed sample.
Sample selectionand preparation
In the period 1945-49,several dozenlazulite specimensobtained frommuseums or individuals, including a number collected in the field byPecora, were examined optically to establish the range in their indices ofrefraction. From these were selectedeight specimensthat demonstrated
a representative distribution over this range.
All the samples were prepared uniformly. Handpicked, visibly purefragments of a single specimen,or adjacent small massesin the matrix ofa single specimen, were crushed so as to pass a 100-mesh screen. The
powdered sample was washed free of dust by repeated decanting withwater. The air-dried 100-200 or 200-300 mesh fractions were purified bymeans of heavy liquids (methylene iodide and acetone) and a Frantz
isodynamic separator. The sample was repeatedly inspected in immersion
Iiquids until a plus-99 per cent purity was established.
The purified sample was divided into two parts. One portion, ranging
from 5 to 25 grams, was used for the chemical analysesand for determination of specificgravity with an Adams-Johnston fused silica pycnometer.
The other portion was retained for precise optical studies. The indices ofrefraction were determined in sodium light and an Abb6 refractometer
was used to check the index liquids for each measurement.
Description of the selectedspecimens
The 8 specimens selected to demonstrate the lazulite-scorzalite
isomorphous series are listed in Table 1, with general information on
locality, habit and occurrence, and mineral association. Two of thespecimensare from Minas Gerais, Brazil, and the others are from theUnited States. All the samples are now deposited with the Curator of
Mineralogy, U. S. National Museum, Washington, D. C.

LA ZU LI TE.SCORZALIT E I SOMORPH OAS SER.TES

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W. T. PECORAAND ]. J. FAHEY

The material from Graves Mountain occurs as well-formed crystals in
quaftzite; two other specimensare from granitic pegmatites and fivefrom quartz-rich veins or dikes in metamorphic rocks.
Dnscnrpuvn Mrxpnerocy
Morphology
Well-formed crystals of lazulite occur at but a few localities. Priifer(1847) described the crystallography of lazulite from druses in quaftz
veins near Werfen, Salzburg, Austria, and Shepard (1859) figured
crystals recoveredfrom quartzite at Graves Mountain, Lincoln County,
Ga. About 16 forms have been reported from theselocalities.Only three

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Frc. 1. Lazulite crystals from Graves Mountain, Ga.,4, view of twinned bipyramidfrom the left side; B, twinned bipyramid from the front; C, tabular habit; and D, twinned
tabular crystal from the right. (Natural size.)

forms are noted in GravesMountain crystals-p(Lfi), e(lll), and l(101).
Dana (1892)and Hintze (1933)summarizethe crystallographyof lazulite
from both localities. The twin laws noted are (223) and (100). Baier(194I) reexamined lazulite specimens from several localities and reported several other twin laws as well.
Lacroix (1926) recorded crystals of lazulite from Madagascar as muchas one centimeterin diameter and similar in habit to the Graves Mountain occurrence. Well-developed crystals are reported by Igelstrcim(1855) as occurring in drusesin vein qlrartz in Horrsjciberg,Wermland,
Sweden.
In the Graves Mountain specimens available for this investigation,
four crystal habits (seeFig. 1) are recognized:(1) bipyramids (p and e),acute or stubby, symmetrical or asymmetrical, with or without a subordinate front dome (t); (2) flat plates, representing malformed crystals
with extension of one pair of pyramidal faces; (3) spindles, representing
malformed crystals with extensionof two pairs of pyramidal facesl andLA ZU LI TE-SCORZA LI TE I SOM ORPH OTIS SBftIES

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W. T. PECORA AND J. T. FAHEV(4) bipyramids with a front reentrant representing crystals twinned on(100), or around the c-axis.In thin section the twin compositionplaneis an irregular, jagged surface essentially parallel to (001).
Most commonly lazulite and scorzalite occur as irregular massesmixed
with other minerals. The mineral breaks with good cleavagealong (110)and (101).As a result most of the grainsin immersionlie so orientedas togive ofi-centered interference figures. Twin lamellae are common in
specimensfrom most localities.
Variotion in chemicalcomposition
Chemical analyses of the 8 selected samples oI lazulite and scorzalite
are listed in Table 2 in the order of their increase in divalent iron. Only
two of these analyses (nos. 6 and 8) have hitherto been published. The
usual methods of analysis were used, except for the determination ofdivalent iron. The members of the lazulite-scorzalite isomorphous series
are so diffi.cultly soluble in the dilute solution of HzSO* and HF used inthis determination that it was necessaryto grind the samples to pass a
300-meshsieve and, further, to collect the undecomposedportion foundin the beaker after titration with permanganate and carry it again
through the procedure. This was repeated as many as three times forthe magnesium-rich members of the series.
For the samplesin Table 2, FeO rangesfrom 2.80to 17.06per cent, andMgO correspondinglyrangesfrom 11.97 to 2.93 per cent. fnasmuch as
MgO*FeO makes up more than 99 per cent of the total RO, the use of
the MgO:FeO molecular ratio is a reliable basis of referenceon which
the variation diagram of the seriesis established.The theoretically pureend members of the serieshave a composition as shown below:

Oxides

Mgo
FeO
Al:O:
PzOs
HrO
Total

Lazulite
MgAlz(POr)z(OH)z

Scorzalite
Fe"Aiz(POr)z(OH)z

46.96
5. 9 6

00.00
21.57
30.54
42.50
5. 3 9100.00100.00

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The specimensselectedfor special study therefore cover a wide enoughrange to establish reasonably the isomorphous series.
In Table 3 are listed 13 additional chemical analyses of lazulite-all
obtained from published sources. These selected analyses include allthat are judged to have been made from reasonably pure samplesas well

LA ZU LI TE.SCORZA LI TE I SOM ORPH OUS SER/ES
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W. T. PECORA AND T, J, FAHEY

as a number of the lessreliable analyses.More than two dozen analysesof lazulite in the literature are of no value in this study becauseof thesignificant amounts of SiOz or CaO reported.
K. J. Murata made a spectrographicstudy of 5 of the samplesshown in
Table 2. His determination of minor elements present in these samplesis
given below:
GravesMt.

ClubbsMt.

.x%Breyfogle
CanyonCorrego
Frio

White
Mt.

Ti

Zn,Mn

Ti

.0x,7,

Ni, Ca, Si, V

Mn, Ca, Si,
V, BA

Mn, Ca, Ba,
Sr, Si, V

Ti, Ca, Si

Cu, Mn, Ni,
Ca, Si, V.0ox7aMn, Zr, Sr,
Cr

Ni, Mo, Zr,
Ga, SrNi, CrNi, Co, Ga

Sr, Cr.000xmoCu, BaCu, CrCr

Co, BaNot foundin any:B, Be,La, Y, Sn,Pb,Ag, Bi, Cd,Ge,In, Tl, Re,Th, U, W, Cb.
Invalid.ity oJ calcium lazulite
Watson (1921), on the basis of 3.12 per cent CaO reported in lazulite
from Graves Mountain, Ga. (Table 3, no. 15), and 2.83 per cent CaO in
Iazulite from Kewatin, Canada (Table 3, no. l2), suggested the namecalcium lazulite to distinguish this variety from calcium-free lazulite.
Meixner (1937), who analyzedseverallazulite specimensfrom Austrian
localities, and Lemmon (1937), who studied lazulite from White Mountain, Calif., both acceptedthe name of calcium lazulite as valid. In 38
chemical analysesof lazulite published prior to 1948, 23 show more than
0.40 per cent CaO and the highest value is 8.20 per cent. The present
writers offer the explanation that the chemical analyses showing asignificant percentageof CaO were probably made on impure samples.
It is noteworthy that CaO is an insignificant constituent in all of thesamples studied by the authors. The new Graves Mountain analysis(Table 2, no.2) shows0.02 per cent CaO; whereasthe original analysis
by Watson (Table 3, no. 15) shows3.12 per cent. The White Mountainanalysis (Table 2, no.7), which shows only 0.02 per cent CaO, likewise
does not support the acceptance of the name calcium lazuliQ used by
Lemmon (1937, p.943) for material from the samelocality.
In the impure fractions recovered by purification of the samples
analyzedfor this paper, such calcium-bearing minerals as calcite, apatite,and garnet are included in the great number of mineral impurities identified. It is likely, therefore, that either or both mineral impurity andLAZULITE-SCORZALITEISOI,IORPHOU,SSERIESI

analytical techniquemay accountfor those chemicalanalysescontaining
significant amounts of CaO.
Seriesnomenclature
The name scorzalite applies only to those members of the isomorphousseries whose Fe:Mg molecular ratio exceeds50:50. Accordingly, theonly three known scorzalite localities are represented by analyses nos.
6,7 , and 8 in Table 2. In theoreticalconsiderations,lazulite and scorzalite
might be usedas namesfor the pure end membersof the series.Following
the usage suggestedby Schaller (1930), ferroan lazulite and magnesianscorzalite are acceptableas names covering the range for the series.Thus
as examples,lazulite from Graves Mountain (Tabie 2, no. 2) is properly
identified as ferroan lazulite (Mgrr:f's1s) and scorzalite from White
Mountain (Table 2, no. 7) as magnesianscorzalite(Mgzz:Feze).
Variation in specif,cgraaity
The specificgravity of the 8 selectedsamples ranges from 3.118 to
3.327. The progressiveincreasein specificgravity for the series,shown in
Fig.2, also is correlatedwith a progressiveincreasein ferrous iron. The
specific gravity of the Chittenden sample is plotted as published andthat for the Stoddard sample was determinedon tvpe material furnishedby T. R. Meyers.
Variotion in optical properties
The indices of refraction of the 8 members of the lazulite-scorzalite
isomorphous serieslisted in Table 2 are plotted in Fig. 2. The progressive
increase in a, B, and .y is correlated with the progressive increase indivalent iron. Birefringencelikewise increasesfrom 0.034 for lazulite to
0.040 for scorzalite.As shown in Fig. 2, the value of (l-ilremains
constant for the series,whereas(B-a) is larger for scorzalite.The valueof 2V is somewhatsmaller for scorzalite.
Data for only two other samplesare plotted in Fig. 2. For one of these-Chittenden, Vt., (Table 3, no. 13)-the indices of refraction were redetermined on a duplicate of the analyzed sample; and for the other
Stoddard, N. H., (Table 3, no. 20)-only a type specimencould be provided for reexamination.Both the published and redetermined values
are listed in Table 3 (and footnote), but the latter only are plotted on
Fig.2.It is unfortunate that preciseoptical data are not given with themany other published analyses.
The absorption and pleochroism of lazulite and scorzalite are among
the most striking found in minerals. With one exception, blue is thedominating color for Y and Z, and X is colorless.Lazulite from Stoddard
is green but blue lazulite is admixed with the green material. The ab-10W, T. PECORA AND J. J. FAHEVLAZ ULl TE --+l-

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numbers are identified in Tables 2 and 3.

sorption formula is the same for all specimens-Z>Y> )X, but thedepth of color for Z andY varies in specimensfrom difierent localities.
Lantlite from Graves Mountain, Dattas, and Clubbs Mountain is light
blue, for example, and the lazulite and scorzalite specimensfrom Cali
fornia are dark blue. There appears to be no definite correlation of color
with composition, although it is noteworthy that the specimensobtained
from quartz veins and dikes are darker blue than those in quaftzite.

LAZULITE-SCORZALITE11

ISOMORPEOUS SERIZS

The dispersion of the optic axes is r1v, perceptible. The orientation,
establishedon oriented thin sections,is: Monoclinic, Y:b; X near c.
Cleavageis good, (110) and (101).
X-ray d.ata
X-ray powder diffraction patterns of the eight samples in Table 2 aresimilar, and each is identified readily as a member of the isomorphousseries. Detailed measurements by J. M. Axelrod of the d-spacings(filtered Cu radiation) of two samplesare given below:
Scorzalite(Corrego Frio)

Laniite(Graves Mt.)

Intensity

Intensity
6.16
4.72
3.60
3.23 (broad)

w
m

J.l+

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m
m

s.07

S

2.55
2.34
2.26
2.22
2.05
2.01
1.977(broad)

w
mw

1.807
r.787
1.684
1. 6 1 8
1.600
1 .568(broad)mw

I. JJ6

r.407
1 .389
1.274
1.185
1.113
.8315(o).8270(a).7836(a).7739(a)mNote: tr:1.5418 (aun.)and 1.5,105(aj.

6.17
4.72
3.60
3.24
3.20
3,L4
3.08
2.55
2.34
2.26
2.22
2.05
2.01
1.989
1.973
1.828
1.811
t.787
1.682
1.622
1.601
1.574(a group)
1.541
1.412
1.390
1.277
1.186
1.115
.8318(ar).8294(a).7849(a).7746(a)

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mw
vw
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mw
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vw
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w
vw
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12

W. T. PECORAAND T. J. FAHEY

The 0.78 A line in the patterns of all the samplesshowsa small variation of spacingwith divalent iron content, as shown below:
Sampl,eGraves Mt.
Breyfogle
Stoddard
Corrego FrioWhite Mt.
Victory

Per centFeO
3.95
8.94
11.58
1 4 . 7+16.27
1 7. 0 6d(A)0.7836
.7844
.7846
.7849
.7856
.7853

The total variation is 0.0020.Interplanar spacingscould be used, therefore, to place a member of the series approximately. Spacing alone
would not give a reliable placement.
Berry (1948) calculated the unit cell for Lazulite and scorzalite fromcleavagepieces as follows:
Unit cell, in A
Locality

1. Werfen, Salzburg
2 . G r a v e sM t . , G a .
3. Churchill River, Canada
4. Corrego Frio, Minas Gerais

7. 1 2
t .l+
/.to
7.15

7. 2 4
7. 2 7
7. 2 5
7. 3 2

7.10
7. 1 6
7.14
7.14

118'55'119018'118"47',
119'00',On the basis of his studies, Berry calculated the theoretical specificgravity of pure lazulite to be 3.14 and pure scorzalite to be 3.39. In
comparisonwith the data plotted in Fig. 2,both of his values are higher
than those obtained by extrapolation of the measuredvalues.
Occunnnrtce
Generalassociation
Laztlite and scorzalite occur in many regions throughout the world
where metamorphic rocks are intruded by granitic rocks. The age ofthese petrogenetic provinces ranges from pre-Cambrian to Cenozoic.
The metamorphic rocks commonly exhibit a high-grade facies of metamorphism and contain veins, dikes, and replacement massesgeneticallyrelated to the granitic rocks of the province.
The phosphate minerals intimately associatedwith lazulite or scorzalite in these regions include apatite, triphylite, wagnerite, berlinite, svanbergite, tetragophosphite, attakolite, kirrolite, trolleite, augelite, brazilianite, souzalite, and other unidentified phosphates.Admixed aluminumrich minerals include kyanite, andalusite, sillimanite, corundum, pyrophyllite, spinel, dumortierite, and garnet. Other associatedminerals are

LAZULITE.SCORZALITEISOMORPHOUS
SERIES

13

quartz, albite, microcline, muscovite, beryl, tourmaline, rutile, ilmenite,hematite, magnetite, pyrite, chalcopyrite, calcite, and aragonite.
Lazulite or scorzalite is a common accessorymineral in several commercially significant nonmetallic mineral deposits. Among these are:(1) mica depositsin the United States, BraziI, and eastern Siberia; (2)andalusite deposits in California and Armenia; (3) diamond and gold
placers in Brazil; (4) sapphire placers in the Himalaya Mountains; and(5) quartz crystal deposits in the Ural Mountains.
On the basis of information in the geological literature and field observations of Pecora, lazulite-scorzalite occurrencescan be conveniently
ciassifiedinto four geological classes:
Class 1. Euhedra and subhedra in quartzite and associatedmetamorphic rocks.
Class 2. Anhedra in quartz-rich veins, dikes, and related replacement
depositsin metamorphic rocks. Euhedra in drusesare rare.
Class 3. Anhedra in granite pegmatites.
Class 4. Abraded fragments in alluvium or colluvium.
These occurrencesare describedbelow with representativelocalities
for each group listed in Table 4.
Occwrrencein quartzile (See Table 4, column 1)
The largest quantity of lazulite occurs in quartzite and quartzitic
schist as individual or bunched grains scattered throughout the rock oralined along quartzitic horizons in a sequenceof foliated rocks. Aluminum-rich silicates and titanium-rich oxides are common mineral associatesin this environment. The quartzite formations in many regions
contain hematite-richbeds.In Madagascar,the lazulite-bearingquartzite
beds are interlayered with dumortierite-rich schist.
Occurrencein quartz-richoeinsand.d,ikes(SeeTable 4, column 2)
Quartz-rich veins and dikes containing lazulite or scorzalite occur inthe same metamorphic rocks describedin Class 1, above, as well as inschist and gneissof other regions.One dike, in Breyfogle Canyon, Calif.,
is reported to be several miles long, and another, at the White Mountain
andalusite mine, is reported to be 300 feet thick. Most veins and dikes
are much smaller. The lazulite or scorzalite occurs as irregular massesin
the quartz or, rarely, as faceted crystals in druses. The quartz is of themassive or comb variety and clear or milky. Andalusite, rutile, kyanite,
muscovite, and pyrophyllite are common mineral associates.Many rare
phosphate minerals occur in the veins and dikes, particularly in Austria,
Sweden,and California. The drusesin the veins in Werfen, Austria, haveprovided many fine crystals of lazulite.

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IV. T, PECORA AND J. J. FAHEY

Occurrencein granitic pegmatites(See Table 4, column 3)
Lazulite or scorzalite in granitic pegmatites selectively occurs in theborder zone rather than in the central zone. This spatial relationshiphas
been already describedby Pecora and Fahey (1948 a and 1948 D). A
number of other phosphateminerals,extremelysodicplagioclase,quartz,
muscovite,tourmaline, and beryl are the common mineral associatesin
this environment. Within regions containing pegmatites, lazulite or
scorzalite is found only in those districts where other phosphate minerals
are abundant. A number of specimenscollectedfrom severalNew Hampshire pegmatites are ferroan lazulite in composition.
Occurrencein alluaium and.collutium (See Table 4, column 4)
Fragments composed of qrartz and lazulite have been recovered in
the diamond-bearingcolluvium near Diamantina, Minas Gerais,and thegem tourmaline district of Mount Bity, Madagascar.Grains of lazulite
have been identified as one of the heavy mineral associatesin diamondand gold placersin Bahia, Brazll, and Belgian Congo,and in the sapphire
placersin northern India.
Gnrr L,czur,rre
The lazulite recovered in many localities, particularly in association
with clear qlrarlz, is of such clarity that it has been cut into gem stones.
Kerr (1926) assignedthe name berkeyiteto gem TazuJite,and this variety
name can apply to gem scorzalite as well.
Acxr.towrnrGMENTS
The authors are indebted to many individuals and institutions for theircourtesy in supplying specimensfor examination and for information concerning localities or specimens.Among the institutions are the U. S.
National Museum, the Philadelphia Academy of Arts and Sciences,
Harvard University, Yale University, University of South Carolina,
Stanford University, California State Bureau of Mines, and the American Museum of Natural History.
Individuals who supplied specimensfor examination include E' R.
S w o b o d a ,B . F . B u i e , C . E . H u n t e r , a n d C . D . W o o d h o u s e .G . E .
Switzer of the SmithsonianInstitution courteouslyaided the writers inassemblingspecimensfrom many localities.
The writers are indebted to a number of their colleaguesin the Geochemistry and Petrology Branch of the U. S. GeologicalSurvey for theirinterest and advice in the course of these investigations.They include
Michael Fleischer,E. S. Larsen,3d, Earl Ingerson,and W. T. Schallerfor
critical suggestions;J. M. Axelrod for f-ray work; K. J. Murata forspectrochemicalwork; and M. L. Lindberg for heavy liquid separations.

LAZULITE.SCORZALITEISOMORPHOUS "'.8R1,8.'

17

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