THE BIOTITE.CORDIERITE-ATMANDITE SUBFACIES OF THEHORNBTENDE.GRANUTITE FACIES

D. on WAARDSyracwse Un'fuer s'i'ty, Syracwse, N . Y., U'5. A.

AssrRAcr

The common, world-wide occurrence of regional-metamorphic quariz-K feldspar-plagioclase-sillimanite-cordierite-biotite-almandite and quartz-K feldspar-plagioclase-cordierite-biotite-almandite-hypersthene assemblages in pelitic gneisses, associated withhypersthene-bearing metabasites, granulites, and charnockites, are characteristic forthe newly established biotite-cordierite-almandite subfacies of the hornblende-granulitefacies.

Coexistence of reactants and products of tjre following two reactions is typomorphicfor the subfacies:

biotite + sillimanite * quartz e cordierite * almandite * orthoclase * HzObiotite + quartz ecordierite + almandite f orthopyroxene * orthoclase * HrO

Equilibrium is a function of FeO/MsO,Ps2o,Prod, and T, and may be considered univari-ant for an open system, or divariant for a closed, H2O-deficient system.

The biotrte-cordierite-almandite subfacies forms the lower Proua (or higher T) portionof the hornblende-granulite facies, bordering on the pyroxene-hornfels facies, and occupy-ing that part of Proua-T conditions in which cordierite and almandite are stable in commonpelitic rocks. Within this stability field of coexisting cordierite and almandite the biotite-iordierite-almandite subfacies borders at lower Ps,o (or higher T) on the cordierite-almandite subfacies of the pyroxene-granulite facies in which hydrous minerals are absent,and at higher Pgre (or lower T) on that part of the almandite-amphibolite facies which ischaracterized by coexisting biotite, cordierite, almandite, and anthophyllite.

Iutnonucrton

Wynne-Edwards & Hay (1963) presented in this magazine valuable

chemical information on the coexisting minerals biotite, cordierite, and

garnet, which occur in pelitic gneisses associated with charnockitic and

granulitic rocks in the Westport area, Ontario. The authors demonstrate

that the assemblage is at equilibrium, and they draw attention to the

world-wide distribution of biotite-cordierite-garnet gneisses in high-grade

metamorphic terranes. Their conclusion is that the association of biotite,

cordierite, and garnet characterizes in pelitic rocks a regional meta-

morphic environment "transitional between those of granulite and high

amphibolite facies" which is not defined by the present facies classification.

The occurrence of cordierite as a stable and widespread mineral in

certain granulite-facies terranes was noted by Eskola (1939)' and the

possibility of a subdivision of the granulite facies based upon the presence

or absence of cordierite has been suggested by Eskola (L952,1957)' and

481

482 THE CANADIAN MINERALoGIST

Turner & Verhoogen (1960). Recently, the establishment was proposedof a biotite-cordierite-almandite subfacies representing the low P1ou6 (orhigh T) portion of the hornblende-granulite facies*, and a possiblecordierite-almandite subfacies of anhydrous assemblages which represenrsthe lower Psr6 (or higher T) conditions of the pyroxene-granulite facies(de Waard, 1965b).

Although there is agreement on the major point, the validity of stablebiotite-cordierite-garnet assemblages as an indicator of a certain meta-morphic environment, the ACF diagram constructed by Wynne-Edwards& Hay differs in some respects from the one proposed by the writer. Thispaper serves to amplify the writer's point of view by considering sevenmineral phases in a six-component system, and to demonstrate therelative P1ou6-Psr6-T conditions of the new subfacies with respect tothose of the four adjoining subfacies.

Ts.n ACFMK Dracneu

Mineral assemblages of analysed cordierite-garnet gneisses and asso-ciated rocks from different high-grade metamorphic terranes of the worldare shown in Table 1; the first ten are those from the Westport area.Wynne-Edwards & Hay attempt to demonstrate that the following three-phase assemblages of the .4CF system can be recognizedt: si-al-ansi-co-al, and bi-co-al. Accordingly, si-al, co-al, and al-bi joins are shownin the ACF diagram.

In the first place it should be remarked that biotite is not properly aphase represented in ACF,because KzO is not a component of this system(eastonitic biotite, when calculated for ACF,will plot in the diagram butis then presented as a rock composed of non-potassic phases such ashypersthene and garnet). Furthermore it is evident from Table 1 thatcordierite-garnet gneisses have essentially the same mineral assemblage,v'iz.,quartz-Kfeldspar-plagioclase-sillimanite-cordierite-biotite-almandite.They cannot be divided into distinct groups, and have to be treated asone six-mineral field: or-an-si-co-bi-al, in addition to excess quattz.A co-an tie line must be present in the ACF diagram because cordieriteand plagioclase coexist in almost all of the cordierite-garnet gneisses,though it may be sparse in several. The ACFdiagram, as it is constructedhere (left triangle in Fig. 1), shows that all of the cordierite-garnetgneisses fall in the an-co-al field.

*In order to avoid having subfacies of subfacies it is suggested here to elevate thehornblende and pyroxene-granulite subfacies (Turner, 1gb8) to the status of facies.

tThe following abbreviations of mineral names are used: qu (quartz), or (K feldspar),an (anorthite), si (sillimanite), co (cordierite), bi (biotite), al (almandite), op (oitho-pyroxene).

BIOTI'I'E-CORDIERITE-ALMANDITE SUBFACItrS 483

The importance of separating FeO and MgO, lumped in the F corner

of. ACF, is properly shown in at AFM diagram in which the minerals

sillimanite, cordierite, almandite, and orthopyroxene are represented, but

not biotite because KrO, also here, is not a component of this system.

In Wynne-Edwards & Hay's AFM diagram most of the rock analyses

fall in the co-al-bi field instead of in the si-co-al field as may have been

expected because sillimanite is present in all but one of the rocks. (Their

diagram is in effect a four-component system in which biotite is projected

on the AFM plane). This failure is partly due to an error in the calculation(subtracting 2CaO from AlzOa), but mainly because of the method of

calculation which translates the AFM components of biotite into non-

potassic phases such as cordierite, almandite, and orthopyroxene, and

into orthoclase which is eliminated by subtracting the molecular amount

of KzO from AlzOs. The only proper method for plotting biotite-bearing

rocks in AFM in order to show their relationship with coexisting phases,

such as sillimanite, cordierite, almandite, and orthopyroxene, is to correct

the values of. A, F,and M for the amount of biotite in the mode.A less

tedious, but also less accurate method, followed here, is to calculate

,4 : AlOa - (NazO * CaO) with the idea that a smaller error is made

by leaving in ,4 the relatively small amount of AlzOa equivalent to KzO

of K feldspar than by subtracting the {airly large amount of AlzOa

equivalent to KzO of biotite. The AFM portion of Fig. 1 shows the

analyses of cordierite-garnet gneisses of Table 1 situated in the si-co-al field.

The AFK diagram demonstrates the composition of rocks rvith respect

to the minerals K feldspar, sillimanite, cordierite, almandite, ortho-

pyroxene, and biotite. All of the cordierite-garnet gneisses, listed in

Table 1, appear to fall in the or-co-al field of the AFK portion of diagram,

Fig. 1. The mineral assemblages in the Table show, however, that both

biotite and K feldspar are present, which is one phase too many for

divariant equilibrium (in AFMK there are two interfering tetrahedrons:

si-co-al-bi, and si-co-al-or). This condition, which is common for the

transition from the almandite-amphibolite facies to the pyroxene-

granulite facies, may be considered to reflect univariant equilibrium for

an open system, or divariant equilibrium for a closed, HsO-deficient

system (de Waard, 1964, 1965a), for the reaction*:

(1) 10 Kz(Fe, Mg)64Al3Si61Ozo(OH)a + 23 AlrSiOu * 65 SiOz <-+

biotite sillimanite qtartz

11 (Fe, Mg)zAlaSioOre * 11 (Fe, Mg)3Al'SiaOrz + 20 KAlsigoa * 20 Hzocordierite almandite orthoclase

*To balance the equations simplified mineral compositions have been chosen which

fairly closely correspond with those known from high-grade metamorphic terranes.

e c cE . n . n

a 'H g- r T bU ' E :

. l i o . =

H -E -.?

3;e8.4 e" - o Xg ? o HM g H*- : r Et r @ Yf i .H I

d ! ] :

t r o a' = ;= ,t r t s 6

- 9 "S . E e

a Aj - o d i

o ! 9 C )O F LA a a6J .- O

: ^ * 9=.* ) :6 E acl bo-

9 ! d

EHEN c d ' =

E * t s

gE F 3. 0 ! E gH , ; E . r

; ; i 5 . ;

? b . 9 F!.) .- * tl

: . 9 U e. : @ . q H

:e.Qx: ! H F

i t 9 . h

d d r 9 {i 9 l b4€F L : . { Ob . 9 E E. s P h kTi F i". ti

5 , 9 6 3R i 5 p 4

U E E q r\ o S lj ? , 9 E. i o h UV - . : E

" $E=

BIOTITE-CORDIERITE.ALMANDITE SUBFACIES

Teer,B 1, MrnBnar- AsssMelecrs oF BrorrrE-ConomnB-GeRNET GNErssEs ANDAssocrerso Rocrs

Mineral assemblage FeO,/FeO*MgO

No. qu or ab an si co bi al LnTo rock

485

albi

45.834.550.450.243 .152.548.254.3

L x x2 x x3 x x4 x x

ir.-. 5 x x6 x x7 x x8 x x9 x x

1 0 x x1 1 x x1 2 x x1 3 x xL 4 x x1 5 x x1 6 x xl T x x1 8 x x1 9 x2 0 x x2 I x -

xxxxxx

:xxxxxxxxxx

xx

x

xx

Ixxxxxxxxxx

xx

1xx

;x

:xxxxxxxxxxx

x x xx x xx - xx x x- x xx x xx - xx x xx x xx x xx x xx x xx x xx x x- x x- x xx x xx x x- x xx x xx x x

45.730.24 8 . 13 8 . 53 9 . 04 r . 756.454.L46.225 .8

34 57 .628 56.4

3H0 52.618 42.923 46.028 56.420 45.223 51 .8

5 6 . 040 56.530 58 .6

29.620.4

34.026.82 7 . 1

67 .4

67 .46 9 . 9

65 .070.7

37 .7 53.4 80.8

32.r 45.8 72.4

73.4

27 .O 63.2

opalno. qu or ab an co bi al op AnVo rock

2 2 x x2 3 x - x x2 4 x x x2 5 x - x

:xx

36 .358 .540.732.7

54.O 35.856 .1 40 .0

Legend: x present, present in very small amounts, - absent or not.reported' FeOofioiks reduied tv TiO, to compensale for ore. Location and source: (1) Southeasterno.t";6, Wynnoeh*utd; & Hai (1963), no. H-29; (2) ibid., no. H-6.0;-(3) ibid., no.H-66: (4) ibid., no. H-70; (5) ibid., no. H-90; (6) ibid., no. H-105; (7) ibid' ' no' H-I26;isl- i l i . i - 'no.1{re-+ss, fs) i6ia., no. WE-10-57; ( lo) i t ia., no. WE-17-57; (I1) -south-i l . i" tn New Hamp"hi ie, Heald (1950), no. LMi; (12) ibid., no. LM6; ( l?) Stqbigcg'nl-.i*.t'"*it", Baiker (tsoz); (t+) Southwestein Finland, Higtanen (194!)'f"Fl" ?'r. . i l t tBl ibid., no. z; '( fo) i6id., no. 3; (17) South Finland, Parras Q958)' Table 2'

". .8d; ' t t t l ibid., no.57; '( tb) Lapland, North Finland, Eskola-(I952), Tatr le.2' no' 11 ;

f-ZOiifia-. ti.. b: eD Souih Coa"t, Weitern Australia, Clarke, Phillips, & Prider (1954),'i.it" ili. r.. C,;r;t"d from Simpson (1951), p. 1o5; (22) Lapland, North Finland'e.[oiu-irss2), fitie l, no.9; (23) ibia., no. 16i Q4) Dangin, WesternAustralia, PriderGda;t T;bt6'lii,

"". zo46ti Esj Mysore, soutl' thaia, Radhakrishna (1954)'Table I'

no.2.

The reaction represents the breakdorvn of biotite in systems with excess

alumina and silica, 'i.e., in common, sillimanite-bearing' pelitic rocks. The

development of coexisting cordierite and almandite, as opposed to that

of cordierite or almandite alone, is a function of P,*d-T conditions and

FeO/MgO ratios of rocks. The left-hand side of the feaction represents

the almandite-amphibolite facies, characterized by coexisting biotite and

sillimanite, and expressed by the dashed tie line in AFK of Fig. 1. The

xxxx

xxxx

15

486 THE CANADIAN MINERALOGIST

right-hand side represents the anhydrous assemblage of the pyroxene-granulite facies, demonstrated by the full-drawn tie lines co-or and al-orin Fig. 1. The combination of reactants and products of the reactioncharacterizes the hornblende-granulite facies,,i.e., the combinationsi-bi-co-al-or in this particular case.

The total number of coexisting minerals demonstrated by the plots ofcordierite-garnet gneisses in Fig. l, ACF: an-co-al, AFM: si-co-al, andAFK: bi-co-al-or, results in the six-phase assemblage or-an-si-bi-co-alwhich, in addition to quartz, are the minerals most commonly representedin the mode.

In pelitic rocks deficient in alumina the Jollowing reaction takes placeinstead of, and presumably at higher T (or lower Pr,6) conditions thanreaction (1):

(2) 6 K2(Fe, Mg)stAl'Sio;Ozo(OH)a + 39 SiO, <-+ (Fe, Mg)rAleSisOr, *biotite qlrartz cordierite

(Fe, Mg)sAlzSisOrz f 28 (Fe, Mg)SiOa + 12 KAlSiaO, * 12HzOalmandite orthopyroxene orthoclase

Four hypersthene-bearing rocks (22-25) , associated with cordierite-garnetgneisses, have been plotted in Fig. 1 to demonstrate the composition ofthis adjoining six-phase field, ACF: an-al-op, AFM: co-al-op, andAFK: bi-or-al-op, rrhich combines to qu-or-an-co-bi-al-op as the maxi-mum number of minerals present in the mode.

TsB BrorrrE-CoRDrERrrE-ALMANDTTE SuBFACTES

The five-component system ACFMK, shown for the biotite-cordierite-almandite subfacies in Fig. 1, is an attempt to illustrate fields of five(six in this case) mineral phases which can be visualized three-dimen-sionally in two stages by combining any two of the three triangles tofour-component tetrahedrons, AFK and AFM are faces of the AFMKtetrahedron in which can be seen the si-co-al-or field in full-drawn tielines, and the si-co-al-bi field in dashed tie lines. ACF and AFM f.ormtwo faces of the ACFM tetrahedron which includes the si-co-al-an field.

In common rock types the following mineral assemblages may beexpected:

(a) qu-or-an-si-co-bi-al(b) qu-or-an-co-bi-al-op(c) qu-or-an-bi-hb-op(d) qu-or-an-hb-op-cp(e) qu-an-bi-al-hb-op

BIOTITE-CORDIERITE.ALMANDITE SUBFACIES 487

Assemblages (a) and (b), depending on the alumina content of the rock,

are found interlayered in pelitic gneisses. Associated charnockites contain

assemblage (c) or (d), depending on the aluminalime ratio of the rock.

Assemblages (d) and (e) occur in basic layers which are common in

charnockitic and pelitic rock units. The combination of hypersthene and

hydrous minerals in assemblages (b), (c), (d), and (e) is characteristicfor the hornblende-granulite facies. Assemblages (c), (d), and (e) may

occur in both the biotite-cordierite-almandite and the hornblende-

orthopyroxene-plagioclase subfacies (see below). Assemblages (a) and (b)

are typical for the biotite-cordierite-almandite subfacies.The relationships between the biotite-cordierite-almandite subfacies

and adjoining subfacies is shown in diagram, Fig.2, as a function of P1*6,

Psr6, and T. Because P and T have opposing effects on the boundary

reactions the three variables can be reduced to the two pressures which

are inversely related to T. The transition from one subfacies to another

may thus be produced also under similar P conditions by a change of T

in the opposite sense from a change of P. The biotite-cordierite-almanditesubfacies occupies the low P66 (or high T) field of the hornblende-granulite facies, borders at higher P66 (or lower T) on the hornblende-

orthopyroxene-plagioclase subfacies, and at lower P66 (or higher T) on

the pyroxene-hornfels facies. At lower Prro (or higher T) it adjoins the

cordierite-almandite subfacies of the pyroxene-granulite facies, and at

higher Pgrs (or lower T) a cordierite-garnet-containing subfacies which

represents the low P,ouo, low Ps2s, or high T portion of almandite-

amphibolite-f acies environments.As a function of Psre-T the boundary between the biotite-cordierite-

almandite subfacies and the upper almandite-amphibolite facies may be

defined by reactions (1) and (2). In view of the more general applicability,

however, the boundary is better defined by the following reaction which

involves the typomorphic assemblages of both the almandite-amphibolite

facies and the pyroxene-granulite facies:

(3) NaCaz(Fe,Mg)rAlssisozz(oH)z * (Fe,Mg)aAlzSiaOrz * 5 Sioz ++

hornblende almandite qlJartz

7 (Fe,Mg)SiOs + NaAlSi'Oa * 2 CaAl$iOs * HrOorthopyroxene plagioclase

According to the reaction the boundary between the almandite-amphibo-

lite facies and the hornblende-granulite facies is delineated in the field

by the first appearance of hypersthene in basic rock types, and the

boundary between the hornblende-granulite facies and the pyroxene-

granulite facies, ideally, by the last occurrence of hornblende in these

rocks. It should be noted that reactions (1), (2), and (3) may vrell be

o

rE

u

ze

; U

,,lt ua <Z LuJ@

zeo

tttJ

U4zeO oE U

.r. u: <uxoe

L

.ll

!

o

,+*

I

' - t - - - (t)(z-t) pDroos!-l-lq-qq- -

u=oo

2 o

r L )H <- L

oz{

qu(J

q

q

:

zeo

(c) Ro,6osr f ao

- oo . -

3 a

o o

a a! i

+ Poo ld

BIOTITE-CORDItrRITE-ALMANDITE SUBFACIES 489

expected to take place at different Prro-T conditions, and that these

conditions for each reaction are influenced by cation ratios of the rock.

The biotite-cordierite-almandite subfacies is distinguished from the

hornblende-orthopyroxene-plagioclase subfacies by the appearance of

cordierite in pelitic rocks (e.g., Scheumann,1925; Scheumann & Hucken-

holz, 1961). The boundary reaction which limits the stability fields of

coexisting femic minerals as a function of FeO/MgO ratios, P1*6, and T

may be conveniently expressed in phases of the AFM system as follows:

,/ "i + co' f al'

(4) si * al + op'l co" f- al't\ aorrr * al" ' + op"'

The boundary between the two subfacies is delineated in the field by a

cordierite isograd which has coexisting cordierite and almandite inpelitic rocks on one side and a consistent absence of cordierite in silli-

manite-biotite-garnet gneisses on the other.The low P66 (or high T) boundary of the biotite-cordierite-almandite

subfacies, and of the hornblende-granulite facies, is marked by the dis-

appearance of almandite in the pyroxene-hornfels facies (4.g., Wheeler,

1e55):

s i f c o f a l \(5) co' + al ' j

" i + co"' I oP't '

cott + al 't ! op't /

The coexistence of biotite, cordierite, and hypersthene characterizes thepyroxene-hornf els f acies.

The biotite-cordierite-almandite subfacies thus occupies a portion of

P6*-T environments in which the stability fields of cordierite and alman-

dite in pelitic assemblages overlap. The subdivision of this cordierite-

almandite field, as shown in Fig. 2, is based upon Prro-T-controlled

dehydration reactions, giving rise to adjoining cordierite-almandite-containing subfacies in the pyroxene-granulite and almandite-amphibolitefacies.

Regional distribution and common occurrence amply evidence the

existence of cordierite-almandite-bearing subfacies. Rocks of the biotite-

cordierite-almandite subfacies, distinguished by bi-co-al-or and bi-co-al-

op-containing assemblages, occur on a regional scale and commonly

Frc. 2. Relationships between metamorphic environments of the biotite-cordierite-almandite subfacies and adjoining subfacies presented as a P1q6-Psro-T controlled,HzO-deficient system for rocks with excess SiOz (T and Proa or Psr6 have opposingefiects on the boundary reactions), Subfacies are represented by ACF-AFK diagramsin which tie lines marked F and. M lndicate the effect of FeO/MgO on the assemblage.

490 THE CANADIAN MINERALOGIST

associated with hypersthene-bearing metabasites, granulites, and char-nockites, e.g., in Ontario, Canada (Wynne-Edwards & Hay, 1963) andin the adjoining northwestern Adirondacks (Smyth & Buddington, 1g26),in western Greenland (Ramberg, 1949), South Norway (Bugge, 1943),South Finland (Hietanen, 1943, 1947; Parras, 1946, 1958), Lapland(Eskola, lg52), Arctic Russia (Rabkin & Ravich, 1960; Bondarenko,1964), the Aldan Shield in Siberia (Marakushev, 1964), Mysore andMadras States in South India (Iyer,1929; Rama Rao, 1945), Ceylon(Cooray, 1963), Western Australia (Prider,.1945, 1958), Central Australia(Wilson, 1960), South Australia (Andrews, 1922; Binns, 1964), andAntarctica (Stillwell, 1918 ; Tilley, 1940 ; McCarthy & Trail, 1963).

The cordierite-almandite subfacies, characterized by the absence ofhydrous minerals in cordierite-garnet assemblages, occurs in the Egersundarea, southwestern Norway (Michot, 1957, 1960). The cordierite-almandite-containing portion of the almandite-amphibolite facies, dis-tinguished by the absence of hypersthene, and the presence of antho-phyllite in cordierite-garnet gneisses and in associated rocks, is found,e.g., in Ontario, Canada (Pye, 1957), South Norway (Bugge, 1943),South Finland (Tuominen & Mikkola, 1950), and Western Australia(Johnstone, 1950).

P-T conditions of the cordierite-almandite-containing subfacies aretransitional into those of the pyroxene-hornfels and hornblende-hornfelsfacies, approximately where the vaguely separated environments ofregional and contact metamorphism meet. Because of these transitionalP-T conditions the subfacies, which are defined by their mineral assem-blages and not by their geologic occurrence, may be found in both regionaland contact-metamorphic environments. The biotite-cordierite-almanditesubfacies occurs predominantly in regional-metamorphic setting, but it isalso represented in some contact-metamorphic aureoles, and in inter-mediate cases it is found on a limited scale in and around plutonic domes,such as the bi-co-al-or-gneiss occurrences in New England (Heald, 1950;Barker, 1961, 1962), which may represent local upward bulges in regional-metamorphic isograd surfaces. An example of the presence of the biotite-cordierite-almandite subfacies in contact-metamorphic aureoles is theoccurrence of bi-co-al-or hornfelses, which developed from medium-graderegional-metamorphic schists, adjacent to the Lochnagar granodioriticintrusions in Scotland (Chinner, 1962).

RrpnnBNcBs

Auonows, E, C. (1922): The geology of the Broken Hill District, Mem. Geol,, Suru, NewSouth Wal'es, Geol,., E, 432 pp.

BIOTI'I'E-CORDIERITE-ALMANDITE SUBFACItrS 49L

BaRr.FR, F. (1961): Phase relations in cordierite-garnet-bearing Kinsman quartzmonzonite and enclosing schist, Lovewell Mountain quadrangle, New Hampshire,Arn. Min.,46, 1166-1176.

--- (1962): Cordierite-garnet gneiss and associated microcline-rich pegmatite atSturbridge, Massachusetts and Union, Connecticut, Am. Min-, 47 ,907-9L8.

BrNNs, R. A: (1964): Zones of progressive regional metamorphism in the WillyamaComplex, Broken Hill District, New South Wales, J. Geol'. Soc. Austral"ia', ll'281-330.

BonoenBNro, L. P. (1964): The granulites and the charnockites of the central qart ofthe Kola Peninsula, XXII Int. Geol,. Congress, Reports of the Sottiet geol'ogists,Problem 1 8, Cbarnoch'ites, Moscms, 1 3-37,

Buccr, J. A. W. (1943): Geological and petrographical investigations in the Kongsberg-Bamble formation, Norges Geol,, Und,ers., 160' 150 pp.

Curwwon, G, A. (1962): Almandine in thermal aureoles, J. Petrol'ogy,3, 316-340.Cr,enrn, E. op C., Purr-r-trs, H. T., & Pntoon, R. T. (1954): The Pre-Cambrian geology

of part of the South coast of western Australia, J. Roy. Soc. Western Austral'im, ?8,1-64.

Coonev, P. G. (1963): The charnockites of Ceylon-a review, Geol'. Soc. Ind"i'o, Sym'pos'i,um on charnockites, Abstracfs, p. 1.

DE WAARD, D. (1964): Mineral assemblages and metamorphic subfacies in the granulite-facies terrane of the Little Moose Mountain syncline, south-central Adirondackhi{hlands, P r oc. K on. N ed,. A kad.. Weten s ch., A msterd.arn, B. 67, 3M-362.

----(1965a): The occurrence of garnet in t}te granulite-facies terrane of the Adiron-dack highlands, J, Petrol,ogy,6, 165-191.

(1965b): A proposed "u6divisiott

of the granulite facies, Am. J. Sci'.,263' 451o-46I'Esror,e, P. (1$9)a Die metamorphen Gesteine, In: Barth, T. F. W., Correns, C' W., &

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Manwscript recehted, June 29, 1965, ernended December 12, 1g6i