The
American Mineralogist, Volume
60,
pages
913918, 1975
XRay Determination of
Axially Symmetric Pole Fabrics from
Interfering Reflections
with Application to Orienting
Mechanisms
in Mica Aggregates
Rosnnr J. Twrssl
euo Ml cH,arnr A. ErHsnroce2
Research
School of Earth Sciences,
Australian National Uniuersity,
Canberra, A.C.T. 2600, Australia
Abstract
The Xray
texture goniometer is widely
used to measure preferred orientations in
pol ycrystal l i ne
materi al s. However, i f the peak
bei ng measured overl aps or coi nci des wi th
another reflection,
the results may be erroneous.
A method is
presented
here which corrects
for the presence
of the spurious reflection in
axially symmetric fabrics, enabling determination
of the true preferred
orientation. The correction ii
applied to two sets of
previously
published
data which give
the
preferred
orientations of experimentally
deformed mica aggregates. The
uncorrected apparently
contradictory results are found
to be closely comparable after correc
ti on, supporti ng the
concl usi on i n one of the papers that the ori enti ng mechani sm
for mi cas i s
mechanical in cold strained
samples and includes effects of crystallization in the hot
strained
sampl es.
Introduction
The Xray
texture
goniometer
is useful in measur
ing the fabric of
a specific mineral
plane
lhkll
:
labcl
in a
polycrystalline
material. If the reflection peak
from
labcl,
however,
closely overlaps peaks due to
other crystallographic planes
Vkn
:
Iatl,
then the
data need to be corrected before interpretation.
Such a situation may be encountered
when measur
ing
the
preferred
orientations of basal planes
in mica.
In
some instruments, the 001 peak is
unsuitable for
such measurements
because of excessive
scattering of
the beam
at low 2d values, and the 003 peak has
to be
used, with its immediately
adjacent 022 reflection.
For example, all
of the
preferred
orientation results
of Means and Paterson (1966)
were determined from
the 003 reflection with a beam
divergence sufficient to
include the whole 022 peak,
This
paper presents
a
correction
procedure
and applies it
to the data of
Means
and Paterson
(1966)
to enable
comparison
with the closely related
work of Etheridge, Paterson,
and Hobbs (1974).
Correction Procedure
Assume the
fabric of the poles to
labclhere
denoted I
labclis
axially symmetric about N (Fig.
I
Now at: Department
of Geology, University of California,
Davi s, Cal i forni a, 95616, U.S.A.
2
Now at: Department of
Earth Sciences, Monash University,
Cl ayton, Vi ctori a 3168, Austral i a.
l). On the unit sphere,
the goniometer inspects a
band so
as
to
detect reflections from those
{abc}
whose poles lie in the band B'. The band has a width
A/ and its median line is defined in terms of the
spherical polar coordinates (@,c.r) by 0
<
Q
3 r/2 and
o
:
0, where
@
:
0 is defined to be the symmetry axis
N.
Consider the small area A, in Bt whose size is
(A/)'
and whose center is at
(@,c,r)
:
(O,0)
where iD is a
par
ticular value of the spherical
polar
coordinate
d.
The
total flux of Xrays f'f'from
planes
whose
poles
are
in l, is the sum of F!;" and F!lp.r, the flux of reflec
tions respectively from
{abc\
and
{aB7}.
Thus
F*"
=
r4, F:A,
(l)
The analysis is easily extended to include more than
the one interfering reflection considered here.
Crystals whose poles I{aB7} lie in I, have their
poles I{aDc} located somewhere in the smallcircle
band B,
(Fig.
l). The
width
of this band is A/. In the
case that
Llabcl
are
not
symmetrically distributed
about
I(aB7) giving rise
to
more
than
one
band
like
By onl of the bands, say the one with the smallest
radius, may be specified.
Consider now an arbitrary area A, within B,
having a size of
(A/)'(Fig.
l). All crystals with l{abc}
in A" willhave
Llalll in a smallcircle band Br. This
band has a width of A/ and necessarily includes
the
area AL. lf we assume no preferred orientation of
Lalll in Bs, then only a fraction of the crystals
913
9t4 R. J. TWISS
AND
Frc.
l.
Geometry
for the correction procedure and tbe spherical
, polar coordinates used in the analysis.
with Llabcl in A, wtll have their Llo,1tl in l'. This
fraction is given by the ratio of the areas of A, to Bt.
At
_
Al'Al
_
Al
t )\
83 Al. C3 C3
\/
where Cg i s the ci rcumference of 8r, and A/ i s smal l.
For ease of anal ysi s, we now i ntroduce a second
spheri cal
pol ar
coordi nate system
({,4)
centered wi th
respect to the smal l ci rcl e band B,
(Fi g.
l ). The coor
di nate
{
i s rel ated
to the fi rst coordi nate system such
that
{
:
0
i s
the same
l i ne
as
(@,c,r)
=
(O,0).
Thi s
l i ne
passes through the center
of
l r. The
coordi nate
4
i s
measured i n a pl ane normal to the l i ne
{
:
0, and the
poi nt
for whi ch
4
:
0 i s taken to l i e on the mi dl i ne of
^Br. Thus the l ocati on of the area Ar, for exampl e, can
be specified
in
both coordinate systems by the respec
ti ve coordi nates (@,c,r) and ({,a) (Fi g. 1). In thi s par
ti cul ar case the second coordi nate system i s set up so
that
f
i s the angl e between Ll abcl and I{aB7} and
hence i s the angl e between the pl anes themsel ves.
Now at any
poi nt (p,p)
i n spheri cal
pol ar
coor
dinates, define a function Inorjt,p) having units of flux
per
uni t l ength by
Fto,
=
Inntj r,p)L/ (3)
Then those crystal s wi th LIabcl i n l, wi l l contri bute
to the flux Fi$' by an amount given by
M. A. ETHERIDGE
, A. f A
6F:;,
:
+ I
l"p.,(t, 1) dC"
:
;
(RF:,',")
(4)
Es
Ja,
D3
where R
:
(F,h/
Foo)
in a uniformly oriented
aggre
gate.
Usi ng
Equati ons
(3)
and
(4),
then,
the total fl ux
due to
L\a/l l i n ,4
'
i s
 A, f
6F:8"
Fle'"
:
Ju,i,"
or,
:R+[,,,,c,i l dC,
( s)
I 5t J
Bo
where
Cg
is the circumference of Br.
Usi ng
Equati ons
(2)
and
(3),
and
wri ti ng the i n
tegrati on expl i ci tl y
gi ves
R f 2"
I oe,(Q,0)
:
= I
I"u"(,
n)
si nl dn
u 3 J o
=
+ t"
I,u,(t,
n)si n{
da
(6)
u3 Jo
where dCz
:
si n{ d4. Now
perform a coordi nate
transformati on
from
({,tl )
to
(@,c^r) to obtai n
t P f o + t Ar
I oa,( e,q:+
I
l"o"( 0,<o) si n 3dd
Q)
L s
J t o  t t
o q
where the l ower l i mi t of i ntegrati on
i s taken as the ab
sol ute val ue because of the
assumed symmetry'of the
fabri c about N.
The two spheri cal
pol ar coordi nate systems are
related by
si n
{
cos
4
=
cos O si n
@
cos cr

si n
s i n{ s i n4
=
s i n@s i nc.r
cos
{
:
sin iD sin
@
cos c,r
* cos
From Equati ons
(8)
and
(9)
sin d sin r,r
t&n q
:
Iot o ti"
O
.*,

tl"
o
"*
O
From Equati on
(10)
cos
{

cos iD cos
S
cos or
:
;_.''
*,i,,
O....'
(12)
[1

cos2
c,r]t/'
:
sin c,r
[si n'
tD 
cos'f

cost
d *
2 cos i D cos{ cosC]t"
srn
(D
si n
@
( 13)
Now
0t annOn
1 6n
0q 6Q

cos'
n
06
O
cos
@
(8)
(e)
A cos
@( 10)
( l
l )
0n
a0
0t ann
,
0 t a n q
:
c o s
4  *
oQ
( 14)
Using Equations (12)
and (13)
to eliminate c,r from
Equat i ons (8) and (11),
and usi ng t he
resul t s i n Equa
t i on
(14),
we obt ai n
0n
do
si n d

[sin'
6

.*t
6

.*;
6r
co
os'litz
( l
5)
Using Equation (15) in
Equation (7) gives
I  o ( Q.0)
:
?4
C"
f **t
1"u.(d,<.,)si nt si nddd
J,
"_r,
lsin'
rD cos'{
cos"
6+
2.oJo
.or!.ffi7t
(1
6)
By di vi di ng
Equati on (l )
by A/, and Equati on (16)
by
A/, the
two equati ons may
be combi ned to gi ve
the
fi nal form
of the desi red equati on
i n uni ts of fl ux per
uni t area (i ntensi ty)
5"a"(Q,0)
:
l r(i D,
0)

?4
c3
f *  t
!"u"( d,o) si nt si n6dd
J,6g1
[ si n'i D
cos"{ cos'd*2
cos e cos{
cos{]'/,
(r7)
where
shh{Q,0):
(l/Al )l net (O,O;
=
(t/Al,)Fi ht (t 8)
The sol uti on
of thi s equati on
may be approxi mated
by breaki ng the
i ntegral i nto a
summati on over a
fi ni te number of i nterval s,
and wri ti ng
an equatl on
for
the i ntensi ty
g"b"(e,O)
i n each i nterval. The
fabri c
has a pl ane
of symmetry normal
to the axi s
of sym
metry
N. Thus when (O +
)
)90.,
the summati on
may be wri tten
i n terms of
the i ntensi ty val ues
between 0o
and 90' onl y. If thi s quadrant
i; di vi ded
i nto (rl ) i nterval s,
we obtai n a set
of n si mul taneous
equat i ons i n n
unknowns
go6"(i Di ),
(i
:
1,2.
..,n).
Cal cul at i ons i n
t hi s paper were
made f or
phl ogopi te
wi th
labcl
:
10031
\o,lyl
:
{022]t
R:0.4
:50o
n:97
usi ng
a computer program wri tten
by R.J. Twi ss.
The
val ue for R
was obtai ned from
yoder
and Eugster
(195a);
{
equal s (001)
A (011) i n phl ogopi t e;
t he val ue
POLE FABRICS
AND ORIENTING MECHANISMS IN MICA
for r gi ves i nterval s
of one degree. Whi l e we di d
not
check the approxi mati on
ri gorousl y for convergence,
empi ri cal l y the behavi or
over the range l 0
<
n
<
9l
i ndi cated
sati sfactory sol uti ons for
the upper l i mi t.
Application
and Results
The probl em
of peak overl ap when
measuri ng mi ca
basal plane preferred
orientations from
00J reflec
ti ons has been
di scussed bri efl y by Etheri dge
et al
(1974).
They stated
that the errors coul d be removed
ei ther by modi fi cati on
of the Xray i nstrument
to
el i mi nate scattered radi ati on
at l ow 2d val ues of
the
goni ometer,
or by the theoreti cal procedure
outl i ned
above. The i nstrument was
accordi ngl y modi fi ed, and
the00l
refl ecti on was used i n al l
thei r measurements,
but the theoreti cal
correcti on was necessary
for com
pari son wi th
the apparentl y confl i cti ng
resul ts whi ch
Means and Paterson (1966)
obtai ned from si mi l ar
ex
periments.
We thus present
corrected 003 daLa from
both studi es, and the measured
001 data from
Etheri dge
et al
(1974)
i n an attempt
to resol ve thi s
conflict.
The
measured Xray i ntensi ty ({y)
at 20
:
26.3.
for the
003
peak
for phlogopite (Yoder
and Eugster,
1954) and
a
gi ven
val ue of i D i s:
g
M(O,0)
:
9,,,(O,0) +9o,,(Q,0)
+
g
B
+
ga
(19)
where 5
s
is the background
intensity extrapolated
to
the peak val ue, and Jo i s
the i ntensi ty of di ffracted
X
rays from the overlapping quartz
til peak (cf
Etheri dge et al, 1974, p.3).
Both 5" and l q are
as
sumed to be i ndependent
of O, and {p can be
measured;
therefore
ga
+
go
has a val ue whi ch
cannot
exceed
the l owest val ue on the measured
i ntensi ty
profi l e
gM
(O,0).
Thi s val ue of J;a occurs
at
(O,0)
:
Gr/2,0).
Thus
gB
+
ga
S ly
(tr/2,0)
lq
3
{* (tr/2,0)'!s
:
!,(20)
Note
that before sol vi ng Equati on (17),
the measured
i ntensi ty val ues
must be corrected
for l q * !8, i.e.,
5r:5u

( 5e t 6s ): { x

6q ( 21)
The preferred
ori entati on i ndex
(rol )
i s cal cul ated
for the corrected intensities using
the following equa
t l on:
s,\3*
POI
:(22)
915
[ o""
!*'si n i D
do
where
!fij*
is the maximum value of 9r,
16,9;
*1.r1"1't
occurs at
O
:
0 and where the i ntegral i n the
denomi 
nator i s
approxi mated by a summati on usi ng
g'oj
(O, 0) and ten
degree steps i n i D.
9t 6 R. J, TWISS AND M. A.
ETHERIDGE
Run T('c) at
P.0.1. cor r ect d P o.I. f or i l st ed val ues of l Q
";1.t.
No
st rai n**
rol l,
o r/:I *t zl t r*t I *t
(oo1)
Te.ste l. Theoretically Corrected Preferred Orientation
In
dices (eol) from Etheridge et al* for Various
Values of ca
A nonzero
value of k
will
always
result in a
higher
value for the corrected
PoI than the uncorrected
pol'
This is clearly
seen in Tables
I and 2 for k
:
0,l/3,
2/3.
r.
The changes i n the
PoI accompl i shed by
the
theoretical
correction for
the
{a0t}
reflections
result
from the different
forms of the functions
5
"8,
(Q) and
{
"r"(Q).
This
is exemplified in Figure
2 for which Js
:
5e
:
0.
The i ntensi ty di stri buti ott
{atc
:9r,
was
assumed,
and the di stri buti ons
fot !op,
:
6
o22and
{7
:
5*,
I 5o,, were calculated
from Equations
(16)
and
(17). The maximum for
5,,
is far removed from that
for
5*, and {7 has a broader
distribution than
grrj
because
of the contribution
of !6,, ' Elimination
of the
!,,r, component increases
the
poI
from 4.6 to 6.8'
The
di stri buti on of
9022,
of
course, i s i nti matel y
rel ated to
that of 9*, by
the structure of the crystal.
As a result,
i f$r, i s uni forml y di stri buted,
then so too
wi l l be
!ou, and we must concl ude
that the magni tude
of
the error
(and
hence
the correcti on) i n
the PoI due to
interference from
022 will decrease
with decreasing
preferred orientation. This behavior
is documented in
Tables I and 2 and displayed
in Figures 3 and
4.
Table I
presents
the
results of a series of experi
ments in
which the preferred orientation
index was
determined
for both tIrc 003 and
the 00,1 reflections.
The results of applying the
theoretical correction to
the
pot
on 003 for
four values of 9q
(for k
:
O,l/3,2/3,1 i n Eq.
23) are al so presented
i n Tabl e I '
The table indicates
that the corrected
pol's
on 00J
conform
most nearl y to the
pot's
on
001 for a val ue
of k
:
2/3.
Figure 3 shows graphically
the relation between
the
pol
on 003, the
preferred corrected PoI on 003,
and
the
pot
on MI . At l ow to
moderate PoI's, the
correc
Tlslr 2. Preferred Orientation
Indices
(eot)
of Means and Pater
son* and Theoretically Corrected
pot
for Various Values of 9q
i:: :l;:l"i:
Si,il,
correc'ied
ll;i;'"',llii;'""';3
""0
r.2
r.8
r.7
2.4
L.2
1.7
r,2 1.4
I.2 1.3
748 25L
751 25L
759 25L
687
500C
589 500C
693 500C
694 500C
700 500c
135 500C
688
500r
691 5001
695 500L
70r 5001
736 500L
r.2
r.2
1.r
3.0
1.8
2.8
2.6
4.9
3.0
4.1
4.9
a.7 1.9
3  7 4,r
2  O 2.3
3.6
3  9
3 .1 3.4
6.2 6.2
I.7 1.9
2 0 2  4
3,9 4.2
4,8
5.0
6.4
6.4
1. 5 2,9
1.5 2 .8
1,3 2,4
2.5 5
.l
4.5
5.0
3.0 4 .1
4  2 4.7
4.0 4 .8
6  2 6 2
2.5 4 ,0
2.9 4.4
4.6 5.0
6.4 6.4
1.4
I.2
t.2
2 3
3.0
6  L
3.4
7.L
7.O
Changes in the
pot
from the
theoretical correction
arise essentially from two
sources. First is the change
introduced by different
possible values ofJq; second
is the
change
introduced by elimination
of the in
terference from
{apl}
reflections.
For the first source, consider
the simplified case for
which,4oB,
:
5n:0.
The intensity curves for 5u and
!r will then differ by the constant amount
!q(Eq.2l)
which can be expressed
(cf Eq. 20) as
{ q:k $x 0Sk Sl
(23)
Using the definition for the
poI
similar to
Equation
(22) and using Equation
(21)'
with Equation
(23), we
pose the problem
?
g^2*
>
g\;'
POI
(corrected) =
:
a r l Au

g^i*
+
k{x
:
PoI
(uncorrected)
Ar * Ao
where Ar and
Au are the total fluxes associated
respectively with 9r and !u through one half of
the
unit sphere, and
An is the difference between these
fluxes. Ap may thus be written
Ao:
*Et he?i dae
et aL
(1,974),
*"
C
,;d L
it
pL! t nt st"ainirE
accwred
contituauslg
ud Ldte res
pectioelA in the tenpe?atwe cucLe.
i l"x= f i M(;12, o)l Rr; i.n.
'l yi s
t he di f f ererce
bet ueen t he ne@wea
intensit! dt o=rlz @d
the bel,grand
Then because
the
pot
i s never l ess than one,
i t must
hol d that
g^:"
POI
(corrected)'
:
:
A c
*Means
and
Patevson
(L966),
**E,
C, a71d. L irpl! st?aining
oearred eely, continuqsT'a' cnd Late'
tespeeti,oeT.y,
in the tape"atwe eacLe.
t 1i.(1Mhl 2, o)t;,
l.n. Txi e t he di f f e"e@e bet Ded t l e neat ured
inteneita
at 6=r/2 and the bacl<gnand.
["'"
nosi nddd
:
k$x
[ o""
"'n6dQ:
k,x
r.4 1.5 2.0 4.4
r.4 1.6 2.O 3.4
1.3 \.4 r.7 3.r
1.9 2.2 2.7 3.7
1,9 2.2 2.6 3.7
3.4 3.8 4.2 4.9
2,2 2,5 3.1 4.4
1.7 1.9 2.5 4 .2
198
25L
209 25L
260 25L
t69 5308
t 99
530E
334 530E
r74 600c
L76
450C
168 530L
216
600r
331
5301
r.7 r.9
L.2 I .3
I .9 Z.r
1.5 3
.3
2.7 3 .8
>
n.:fr'
!.0!.
:
ry
=
por
(uncorrected)
:
A"+k l x AM
POLE
FABRICS AND ORIENTING
MECHANISMS IN MICA
ti on to the
por
on 003 reproduces
sati sfactori l y the
pol
on 001. The
correspondence
i s not as good at
hi gher
por,
but the correcti on i s i n the ri ght
di recti on
and i n general
mi ni mi zes the change i n
the
por.
The
di screpancy
may be accounted for at l east i n part
by
the fact that i n
sampl es havi ng a hi gh
por,
the con
tri buti on
to !y
Qr/2,0)
from {n,, and{
o,i s
smal l,
and
even though
the absol ute
amount of quartz present
i s
smal l, 9q wi l l
be a fracti on (k)
of
(S
u(T /2,0)Js)
whi ch
approaches
one. Thus the use
of k
:2/3
to correct
al l
pot's
i s a compromi se whi ch
works l east wel l for hi gh
val ues
of the
por.
The most
si gni fi cant fact demonstrated
by Fi gure
3, however, i s
that the correcti on wi th
k
=
2/3 suc
cessful l y and
accuratel y i ncreases
the di sti ncti on
between
the
por's
for the col d
and the hotstrai ned
sampl es.
Table 2 presents
corrections for some
of Means
and
Paterson's (1966)
data sel ected to represent
the
range
of thei r reported
por
val ues. The
data were
taken from
the ori gi nal Xray
charts ki ndl y provi ded
by Dr. Paterson.
Agai n four val ues of
gq
were used to
produce
a range
of
possi bl e
resul ts.
Discussion
Means and Patterson (1966)
concl uded that the
pot's
on al l of thei r speci mens are i ndi sti ngui shabl e,
and that
therefore the ori enti ng mechani sm
for the
pl aty mi neral s, whi ch
can be onl y mechani cal
rota
ti on i n the col dstrai n
experi ments, must be the
same
for al l thei r experi mental
condi ti ons. Fi gure 4a pre
sents the
pol's
determined
from 00l reflections in
phl ogopi te
sampl es as reported
i n Means and
Paterson
(1966),
Tabl e l.
The l ack of separati on
between thei r col d and hotstrai ned
sampl es seems
to
j usti fy
thei r concl usi on. The
resul ts of our
theoreti cal
correcti on to the data, however,
requi re a
di fferent concl usi on.
Table 2 presents
selected data from Means
and
Paterson's
(1966)
Tabl e I
al ong wi th the resul ts
of
our theoreti cal correcti ons
to those data. The most
appropri ate
val ue of Jq for accuratel y
correcti ng l ow
to moderate
eoI's appears to be {q
:
2/35*. Thi s i s
indicated by the
experimental check on the
correction
di scussed above and
tabul ated i n Tabl e l.
Figures
4b and c are histograms plotted
from Table
2 of the uncorrected
por's
and the
pot's
corrected
wi th
k
:
2/1. These fi gures
show that the measured
range
of
poI's
of Means and Pat erson (1
.2

2.8) i s
si gni fi cantl y
expanded
(1.5

4.2), and
the di sti ncti on
between the col d
and hotstrai ned sampl es
i s si gni fi 
cantl y i ncreased. Al though
stati sti cal
anal ysi s of the
o t o 2 0 3 0 4 0 5 0 6 0 7 0 8 0 9 0
l,
=
loor+ !o""
ANGLE
(D
Frc. 2. Effect of interfering reflections
on the true intensity dis
t ri but i on.
data in Figures 3 and 4 is not warranted, the
in
terpretations
given
are consistent with the results of
l
tests for
the significance of the difference in mean
values
of the hot and coldstrained samples using
Equat i on 11.2.5
i n Freund
(1971).
Means and Paterson's
runs 198. 209. and 260
(Table
2), which were heated
first and then strained at
25"C, are all at the low end
of the
por
distribution,
comparing closely with similarly deformed
specimens
of Etheridge
et al
(1974) (e.9.,
748, 7 51, 7 59,Table
l).
Most of Means
and Paterson's runs strained at high
temperatures are at
the high end of the distribution.
These are very similar
to comparably deformed
specimens of
Etheridge et al
(1974) (Table
1).
lo""
2 y
.r
I F
> l 
F L
a
z
U
z
DATA FROM TABLE I
A POI on
( 0O3)
C P 0 I o n
( oo
r )
l c oLD
STRAI NED s aMpLEs
n
s ot s t RAt NEo s AMpLEs
Frc. 3. Values
of the preferred
orientation index (eor) from
Table I Lines
between histograms connect values
for the same
sample A.
por
determined
on 00i reflections;
B.
ror
from
(A)
after
theorectical correction
with &
:
2/3;
C.
por
determined on 00i
reflections.
UNCORRECTED PO.t.:4
6
CORREC ED POI
:
6 A
918
DATA FROI/I MEANS AND PATERSON, TABLE I
R. J.
TWISS AND M. A. ETHERIDGE
9
8
7
6
5
3
2
B POI o n
( O0 3 )
Cor r ect ed POI
for IO=
2,/rl r1
40 45 50 55 60 65 70 7.5
I coLo
sr RAr NEo saMPLES
!
Hor sr RAt NEo sAMpLEs
FIc. 4. Values of the
preferred
orientation
index (not). Lines
between histograms connect
values for the same sample. A.
rot
determined from 003
reflections as reported by Means and
Pat erson
(1966), Tabl e l. B.
pol
sel ect ed f rom
(a)
See
Tabl e 2. C
pot
from (b) after theoretical correction with k
:
2/3. See
Table 2.
It i s thus concl uded that there i s a
si gni fi cant
difference between the mica
{001}
preferred orienta
t i ons of t he hot (500"C) and col d
(25')
st rai ned
speci mens of Means and Paterson.
These
data
appear
to i nval i date thei r concl usi on about the
ori enti ng
mechani sm for the hot strai ned sampl es.
Thei r cor
rected results
are closely comparable
with those of
Etheri dge
et al (1974) and thus
are consi stent
wi th the
concl usi ons
of the l atter
that al though the
l ow
temperature orienting
process for
phlogopite does in
deed i nvol ve mechani cal
rotati on, the
hi ghtempera
ture ori enti ng
processes i nvol ve the
i nteracti on of
ani sotropi c
growth rates wi th any or
al l of the fol 
l owi ng: ani sotropi c
fl ui d movement,
ani sotropi c pore
structure,
and the crystal l ographi c
ani sotropy of
"pressure sol uti on."
Acknowledgments
We woul d l i ke to
thank B. E Hobbs, G. S.
Li ster, and M S'
Paterson for comments
and discussion
throughout the work'
W. D. Means first
pointed out the
possibility of interfering reflec
tions in his XraY
measurements.
This
work was done while Twiss held
a NATO Postdoctoral Fel
towship
at the Australian National
University. This support
is
gratefully acknowledged.
References
ETHERTDGE, M A., M. S.
P,+rersoN, eNo B. E'
Hoaas (1974) Ex
perimentally
produced preferred orientation
in synthetic mica
aggregates.
Contrib. Mineral Petrol.
44' 2'75294'
FREUND, JonN
E. (1971) Mathematical
Statistics, PrenticeHall,
I nc.,
Engl ewood Cl i f f s, N.J',
463
P.
MnnNs, W D., er.rn M.
S. P,'\rsnsoN (1966) Experiments
on
preferred orientation of
platy minerals Contib
Mineral Petrol'
13,108 133.
Yoorr.. H. S..
nNo H. P. Eucsrnn
(1954)
Phl ogopi te
synthesi s and
stability range. Geochim.
Cosmochim.
Acla, 6, 157185'
Manuscript receiued, Nouember
I, 1974, accepted
Jbr
publication, MaY 5, 1975
1[
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