Eos, V o l . 67, N o . 9, March 4, 1986
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n e w j o u r n a l called Global Biogeochemical Cycles
(which covers it all), a n d t h e r e was t h e wella t t e n d e d E a r t h System Science: N e w Views
a n d Plans s y m p o s i u m at t h e 1985 A G U Fall
m e e t i n g in S a n F r a n c i s c o , Calif., last D e c e m ­
ber.
W h y all t h e i n t e r e s t in t h e global scale? It's
safe to say t h a t t h e i m p o r t a n t p r e s e n t c o n ­
c e r n s of t h e e a r t h sciences, s u c h as climate
stability a n d t h e o c e a n ' s c o n t i n u e d p o t e n t i a l
to a b s o r b civilization's c h e m i c a l wastes, a r e
global issues a n d m u s t be viewed in t h a t c o n ­
text if we a r e to a d d r e s s t h e m p r o p e r l y . A n ­
o t h e r factor is t h a t for t h e first t i m e , t h r o u g h
satellite t e c h n o l o g y , we h a v e t h e capability of
g a t h e r i n g global scale d a t a o n a truly synoptic
basis. So, as in t h e past, a p p l i c a t i o n of n e w
t e c h n o l o g y allows u s to d e f i n e n e w h o r i z o n s
a n d a d d r e s s a n e w r a n g e of r e s e a r c h q u e s ­
tions. I n a d d i t i o n to t h e s e factors, t h e r e is
also t h e historical e v o l u t i o n of o c e a n o g r a p h y ,
w h i c h m a k e s t h e global p r o s p e c t i v e p a r t i c u ­
larly a p p e a l i n g at this t i m e .
T h e scientific e x p l o r a t i o n of t h e o c e a n in
t h e late 19th a n d early 2 0 t h c e n t u r y was
d o m i n a t e d by g r e a t n a t i o n a l e x p e d i t i o n s t h a t
gave us t h e first g l i m p s e of vast a r e a s of t h e
o c e a n . As t h e m o s t g e n e r a l p i c t u r e of t h e
o c e a n ' s large-scale s t r u c t u r e e m e r g e d , a t t e n ­
tion was d i r e c t e d t o w a r d s specific r e g i o n s of
t h e o c e a n , s u c h as t h e G u l f S t r e a m , u p w e l l i n g
r e g i m e s , etc., t h e field of r e g i o n a l o c e a n o g r a ­
p h y evolved. N o w a r m e d with a r e a s o n a b l y
g o o d p i c t u r e of t h e r e g i o n s a n d with t h e n e c ­
essary t e c h n o l o g y to view t h e global in its e n ­
tirety, we a r e g u i d e d t o w a r d t h e i m p o r t a n t
global scientific c o n c e r n s of t o d a y . It's t i m e to
p u t t h e r e g i o n a l pieces of t h e j i g s a w puzzle
t o g e t h e r to d e t e r m i n e h o w t h e y i n t e r a c t with
o n e a n o t h e r a n d with t h e a t m o s p h e r e in es-
;
Eos, Vol. 67, N o . 9, March 4, 1986
SOUTHERN
OCEAN
NORTH
THE TWO GLOBAL SCALE THERMOHALINE
ATLANTIC
CELLS
Fig. 1. S c h e m a t i c r e p r e s e n t a t i o n of t h e
two d o m i n a n t global scale t h e r m o h a l i n e
circulation cells a l o n g a m e r i d i o n a l p l a n e .
T h e m a g n i t u d e of t h e f o r m a t i o n r a t e s of
Antarctic Bottom water a n d N o r t h Atlan­
tic D e e p w a t e r a r e " b a l l p a r k " values.
tablishing t h e climate system, its stability a n d
variability, a n d t h e delicate b a l a n c e of t h e
global b i o g e o c h e m i c a l system.
W i t h all this i n t e r e s t a b o u t t h e global scale,
it's n a t u r a l to ask: Is t h e r e really a global
scale o c e a n circulation? H o w a r e t h e r e g i o n a l
circulation cells l i n k e d t o g e t h e r ? W h i l e t h e
r e g i o n a l systems a r e g e n e r a l l y t h o u g h t to be
w i n d - d r i v e n f e a t u r e s , t h e global scale circula­
tion is of t h e m o r e sluggish t h e r m o h a l i n e cir­
culation t y p e , d r i v e n by large-scale b u o y a n c y
fluxes b e t w e e n o c e a n a n d a t m o s p h e r e .
P e r h a p s t h e m o s t influential global scale
t h e r m o h a l i n e circulation t h e o r y is t h a t for t h e
abyssal circulation, p r o p o s e d by Stommel and
Axons [ I 9 6 0 ] . T h i s e n d u r i n g yet s i m p l e con­
cept, in w h i c h s t r o n g m e r i d i o n a l flow within
t h e w e s t e r n b o u n d a r i e s of t h e o c e a n is bal­
a n c e d in b o t h mass a n d vorticity by t h e slug­
gish i n t e r i o r flow, h a s b e e n well verified by
o b s e r v a t i o n s . It h a s b e e n e x t e n d e d , u s i n g
m o r e realistic o c e a n b a t h y m e t r y , a n d its valid­
ity to o c e a n b a s i n - r i d g e scale has b e e n estab­
lished ( d u e largely to t h e w o r k of B r u c e W a r ­
r e n of W o o d s H o l e O c e a n o g r a p h i c Institu­
tion, W o o d s H o l e , Mass.).
T h e global p r o s p e c t i v e is often t a k e n in
s t u d y of t h e s o u t h e r n o c e a n , w h e r e t h e m a j o r
o c e a n s a r e linked by t h e d e e p r e a c h i n g circum a n t a r c t i c belt in t h e 5 0 ° - 6 0 ° S r a n g e . W i t h ­
in this belt is t h e e a s t w a r d flowing A n t a r c t i c
C i r c u m p o l a r C u r r e n t . P e r h a p s it's u n f a i r to
call this a global c u r r e n t , since it encircles t h e
l o n g i t u d e s at h i g h l a t i t u d e s , b u t it s h o u l d b e
n o t e d t h a t with its p a t h of 2 4 , 0 0 0 k m a n d
t r a n s p o r t of 125 Sv (Sv = 1 0 m / s ) it is t h e
s t r o n g e s t , m o s t d o m i n a n t c u r r e n t of t h e
w o r l d o c e a n . It is t h e m o s t i m p o r t a n t factor
in d i m i n i s h i n g t h e differences b e t w e e n
o c e a n s . H o w e v e r , this is p r o b a b l y b e c a u s e it is
t h e t h e r m o h a l i n e p a r t of t h e s o u t h e r n o c e a n
t h a t h a s t h e g r e a t e s t i m p a c t at t h e global
scale. I n t e n s e w a t e r m a s s a l t e r a t i o n a r o u n d
A n t a r c t i c a o c c u r s as t h e relatively w a r m Cir­
c u m p o l a r D e e p w a t e r upwells to i n t e r a c t with
t h e p o l a r a t m o s p h e r e , t h e sea, a n d t h e glacial
ice to f o r m d e n s e A n t a r c t i c B o t t o m w a t e r .
T h i s w a t e r mass c r e e p s n o r t h w a r d , r e a c h i n g
well i n t o t h e n o r t h e r n h e m i s p h e r e . It has
b e e n said (in partial j e s t , of course) t h a t t h e
Atlantic, Pacific, a n d I n d i a n o c e a n s a r e m e r e
e s t u r a r i e s of t h e s o u t h e r n o c e a n .
6
3
H o w e v e r , t h e global s p r e a d of A n t a r c t i c
B o t t o m w a t e r is n o t t h e only t h e r m o h a l i n e
"show in t o w n . " T h e r e a r e two global scale
circulation cells ( F i g u r e 1), o n e c o m p o s e d of
A n t a r c t i c B o t t o m w a t e r , c o m p e n s a t e d by r e ­
t u r n to t h e s o u t h e r n o c e a n as t h e s o m e w h a t
w a r m e r saltier C i r c u m p o l a r D e e p water, a n d
t h e o t h e r d r i v e n by N o r t h Atlantic events, as
u p p e r layer o r t h e r m o c l i n e w a t e r is c o n v e r t e d
to N o r t h Atlantic D e e p w a t e r ( N A D W ) . T h e
full e x t e n t of t h e N A D W / t h e r m o c l i n e t h e r ­
m o h a l i n e cell has n o t really b e e n e x p l o r e d in
t h e l i t e r a t u r e , a l t h o u g h t h e global s p r e a d i n g
of t h e salinity m a x i m u m of N A D W [Reid and
Lynn, 1971] is firmly p a r t of i n t r o d u c t o r y
c o u r s e s of Physical O c e a n o g r a p h y .
As N A D W s p r e a d s t h r o u g h o u t t h e o c e a n ,
slow u p w e l l i n g r e t u r n s w a t e r to t h e u p p e r
layer (a la Stommel and Arons [I960]) which
initially fed t h e initial p r o d u c t i o n of N A D W .
N a t u r a l l y , t h e u p p e r layer water m u s t flow
back to t h e N o r t h Atlantic to b a l a n c e t h e ex­
p o r t of d e e p w a t e r . T h i s t h e r m o h a l i n e cell is
so well d e v e l o p e d t h a t it is clearly seen in t h e
inverse s o l u t i o n s for N o r t h Atlantic t r a n s p o r t
a l o n g t h e m e r i d i o n a l p l a n e [Roemmich and
Wunsch, 1985]: u p p e r layer water within t h e
t h e r m o c l i n e flows n o r t h w a r d to b a l a n c e a p ­
p r o x i m a t e l y 17 Sv of s o u t h w a r d t r a n s p o r t
within t h e d e e p w a t e r . T h i s f e a t u r e m u s t be
p a r t of a global system; h o w e v e r , t h e p a t h of
t h e r e t u r n flow h a s n o t b e e n identified. A
clue exists within t h e S o u t h Atlantic: o c e a n i c
h e a t flux across 30° S is d i r e c t e d t o w a r d t h e
e q u a t o r (talk a b o u t t a k i n g coals to Newcastle)!
A c c o r d i n g to Hastenrath [1982] at a r a t e of 6 9
x 1 0 W. Since it is n o t likely t h a t this h e a t
is i n t r o d u c e d to t h e Atlantic from t h e a t m o ­
s p h e r e s o u t h of 30°S, w h e r e d o e s it c o m e
f r o m ? I believe it c o m e s f r o m t h e I n d i a n
O c e a n t h e r m o c l i n e a n d is p a r t of t h e global
scale N A D W / t h e r m o c l i n e circulation cell.
1 3
If realistic values for N A D W t e m p e r a t u r e
a n d v o l u m e flux (2°C a n d 17 Sv, respectively)
a n d for t h e Brazil C u r r e n t flow across 30°S
(18°C a n d 10 Sv, respectively; see Gordon
[1986]) a r e u s e d , it can be seen t h a t t h e
n o r t h w a r d flowing u p p e r layer w a t e r m u s t
have a n a v e r a g e t e m p e r a t u r e of 12°-14° C,
far t o o w a r m to b e d e r i v e d f r o m t h e D r a k e
Passage. It c a n only be d e r i v e d f r o m t h e I n ­
dian Ocean. An Indian Ocean thermocline
s o u r c e for this u p p e r layer flow is s u p p o r t e d
by r e c e n t o b s e r v a t i o n s t h a t indicate l e a k a g e
of t h e A g u l h a s C u r r e n t (within t h e w a r m e r
u p p e r layers) to t h e S o u t h Atlantic s u b t r o p i ­
cal g y r e [Gordon, 1985], a l t h o u g h m o s t (80—
©
UPWELLING
SINKING
DEEP WATER FLOW
COLD"WATER T R A N S F E R
INTO A T L A N T I C OCEAN
"WARM"UPPER LAYER FLOW
Fig- 2-
M a p view of t h e N o r t h Atlantic D e e p w a t e r t h e r m o c l i n e circulation cell [Gordon, 1986]. T h e circled values r e f e r to t r a n s p o r t in
S v e r d r u p u n i t s r e q u i r e d to m a t c h globally u n i f o r m u p w e l l i n g of a 20-Sv p r o d u c t i o n of N A D W .
Eos, V o l . 6 7 , N o . 9, March 4, 1 9 8 6
90%) of t h e A g u l h a s flow curls back i n t o t h e
I n d i a n O c e a n as p a r t of t h e A g u l h a s R e t r o flection. T h e s u b t r o p i c a l g y r e of t h e S o u t h
Atlantic is m o s t u n i q u e in t h a t t h e r e is a h e a t
s o u r c e at its p o l e w a r d - e a s t e r n c o r n e r a n d as
Olson and Evans [1986] p o i n t o u t , t h e A g u l h a s
c o n n e c t i o n also m a y s u p p l y significant
a m o u n t of anticyclonic vorticity i n t o t h e
S o u t h Atlantic.
W i t h a n I n d i a n - A t l a n t i c t h e r m o c l i n e link in
m i n d , a global p a t t e r n for t h e N A D W t h e r ­
mocline circulation cell is p r o p o s e d ( F i g u r e 2;
See also Gordon [1986]): N A D W s p r e a d s into
each o c e a n , w h e r e it is e v e n t u a l l y i n t r o d u c e d
into t h e t h e r m o c l i n e (it is likely t h a t t h e u p ­
welling a r o u n d A n t a r c t i c a a n d t h e p r o d u c ­
tion of A n t a r c t i c i n t e r m e d i a t e w a t e r plays a n
i m p o r t a n t role), a n d t h e t h e r m o c l i n e w a t e r
b e g i n s its l o n g t r i p b a c k to t h e N o r t h Atlantic
to c o m p l e t e t h e cycle.
T h e N A D W , e n t e r i n g t h e Pacific t h e r m o ­
cline, feeds w e s t w a r d flow i n t o t h e I n d i a n
O c e a n t h r o u g h t h e I n d o n e s i a n seas. Esti­
m a t e s of t h e v o l u m e flux r e p o r t e d in t h e lit­
e r a t u r e h a v e a n o r d e r to m a g n i t u d e r a n g e :
1.5 Sv [Wyrtki, 1961] to 14 Sv [Poila and Gor­
don, 1984]. D u r i n g t r a n s i t of t h e I n d o n e s i a n
seas t h e r e is e v i d e n c e of a n o m a l o u s l y h i g h
vertical m i x i n g within t h e t h e r m o c l i n e : t h e
surface w a t e r t e m p e r a t u r e d e c e a s e s d e s p i t e
s t r o n g a t m o s p h e r e t o o c e a n h e a t flux. T h e
N o r t h Pacific s u b s u r f a c e salinity m a x i m u m is
a n n i h i l a t e d d u r i n g p a s s a g e , a n d t h e vertical
n u t r i e n t g r a d i e n t across t h e t h e r m o c l i n e is
greatly r e d u c e d . T h e Pacific to I n d i a n t r a n s ­
fer of tropical w a t e r a n d t h e s t r o n g vertical
m i x i n g within t h e I n d o n e s i a n seas s h o u l d
h a v e s o m e i m p o r t a n t larger-scale effects o n
t h e h e a t , fresh w a t e r , a n d n u t r i e n t b u d g e t s .
T h e s p r e a d of t h e low-salinity Pacific w a t e r
across t h e e n t i r e I n d i a n O c e a n a l o n g 10° S is
clearly seen in t h e v a r i o u s t h e r m o c l i n e m a p s
p r e s e n t e d by Wyrtki [1971]. T h e similarity of
t h e t h e r m o c l i n e within t h e I n d i a n O c e a n
n o r t h of 10° S in r e g a r d to t h e low vertical sa­
linity g r a d i e n t a n d h i g h n e a r - s u r f a c e n u t r i e n t
c o n c e n t r a t i o n s suggests s o m e c o n n e c t i o n with
t h e I n d o n e s i a n flow-through a n d m i x i n g
event. H o w e v e r , t h e Pacific-derived w a t e r in
t h e tropical I n d i a n O c e a n eventually slips
southward through the Mozambique Channel
to feed (as a m i n o r c o m p o n e n t ) t h e A g u l h a s
C u r r e n t , which in t u r n i n t r o d u c e s I n d i a n
O c e a n t h e r m o c l i n e w a t e r into t h e S o u t h At­
lantic. W h i l e t h e p o l e w a r d flux within t h e
M o z a m b i q u e C h a n n e l is s u g g e s t e d by t h e wa­
ter mass characteristics, t h e r e is n o s t r o n g evi­
d e n c e t h a t t h e r e is a p o l e w a r d mass flux at
t h e a p p r o x i m a t e l y 10-Sv level, as r e q u i r e d by
t h e global scale p a t t e r n .
O n c e in t h e Atlantic, t h e u p p e r layer t h e r ­
mocline w a t e r passes to t h e n o r t h within t h e
subtropical g y r e a n d crosses t h e e q u a t o r ,
p r o b a b l y o n t h e w e s t e r n side, a l t h o u g h s o m e
i n v o l v e m e n t with t h e c o m p l e x vertical a n d
zonal e q u a t o r i a l circulation is possible. T h e
Caribbean a n d Gulf Stream features carry the
thermocline water further n o r t h into the
N A D W production regions.
T h e p r o p o s e d N A D W / t h e r m o c l i n e cell in­
volves m u c h of t h e t h e r m o c l i n e circulation.
T h e efficiency of t h e system, a n d p e r h a p s t h e
vigor of N A D W p r o d u c t i o n itself, m a y d e ­
p e n d u p o n t h e ability of t h e system to pass
t h e r m o c l i n e w a t e r b e t w e e n o c e a n basins.
T h e s e links m a y be v u l n e r a b l e to variations
d u e to t h e w i n d - d r i v e n circulation. T h e Pacif­
ic O c e a n to I n d i a n O c e a n sea level difference
0 0 9 6 - 3 9 4 1 / 8 6 / 6 7 0 9 - 0 1 1 0 $ 1.00
Copyright 1 9 8 6 by the A m e r i c a n Geophysical U n i o n
across t h e I n d o n e s i a n seas m i g h t vary as t h e
large-scale w i n d fields o v e r t h e tropical Pacif­
ic a n d I n d i a n o c e a n s c h a n g e , p e r h a p s in r e ­
s p o n s e to S o u t h e r n Oscillation e v e n t s . T h e
l e a k a g e of I n d i a n O c e a n t h e r m o c l i n e w a t e r
into t h e S o u t h Atlantic is effected by t h e local
w i n d : m o d e l s show t h a t t h e l e a k a g e g r o w s
l a r g e r as t h e m a x i m u m westerlies shift fur­
t h e r to t h e s o u t h . T h u s t h e s e two links m a y
act as " c h o k e " p o i n t s , w h i c h u p o n r e s p o n d i n g
to t h e wind affect t h e e n t i r e efficiency of t h e
t h e r m o h a l i n e cell. C l i m a t e variability at a va­
riety of t i m e scales m a y b e r e l a t e d to t h e im­
p o s e d w i n d d r i v e efficiency of this cell a n d
b e a r s investigation. W i t h a global p r o s p e c t i v e
in m i n d , t h e o c e a n o g r a p h y of c e r t a i n r e g i o n s ,
while i n t e r e s t i n g in its o w n r i g h t , takes o n
n e w significance. I n t h e s c h e m e p r e s e n t e d
above, it is s u g g e s t e d t h a t ventilation of s p e ­
cific t h e r m o c l i n e s m a y n o t b e successfully a p ­
p r o a c h e d in isolation f r o m n e i g h b o r i n g t h e r ­
moclines.
W e a r e a b o u t to e n t e r i n t o a n e w p h a s e of
o c e a n o g r a p h y as we t a k e o n t h e global p r o ­
spective. A r m e d with g o o d k n o w l e d g e of r e ­
gional o c e a n o g r a p h y a n d with t h e t e c h n o l o g y
available to us, I suspect t h a t by t h e y e a r
2 0 0 0 we will b e a m a z e d to l e a r n t h a t all t h e
t h i n g s t h a t we h a v e b e e n saying a b o u t t h e im­
p o r t a n c e of t h e o c e a n to large-scale climate
system a r e really t r u e ! Well, w h a t ' s left for
t h e 21st c e n t u r y ? I n a d d i t i o n to s e t t i n g m o n i ­
t o r i n g n e t w o r k s to k e e p tabs o n t h e o c e a n , I
guess we will g o back a n d get t h e r e g i o n a l
and process oceanography d o n e right, and
t h e n t h e r e ' s always t h o s e o t h e r b o d i e s in t h e
solar system, with liquid a n d ice " o c e a n s . "
T h i s w o r k was p r e s e n t e d at t h e A G U /
A m e r i c a n Society of L i m n o l o g y a n d O c e a n ­
o g r a p h y O c e a n Sciences M e e t i n g L u n c h e o n ,
N e w O r l e a n s , La., J a n u a r y 15, 1986.
References:
G o r d o n , A., I n d i a n - A t l a n t i c t r a n s f e r of t h e r ­
m o c l i n e w a t e r at t h e A g u l h a s Retroflection,
Science, 227, 1030, 1985.
G o r d o n , A., I n t e r o c e a n e x c h a n g e of t h e r m o ­
cline w a t e r , J. Geophys. Res., in p r e s s , 1986.
H a s t e n r a t h , S., O n m e r i d i o n a l h e a t t r a n s ­
p o r t s in t h e w o r l d o c e a n , J. Phys. Oceanogr.,
12, 9 2 2 , 1982.
O l s o n , D., a n d R. E v a n s , R i n g s of t h e A g u l ­
h a s C u r r e n t , Deep Sea Res., in p r e s s , 1986.
Piola, A., a n d A. G o r d o n , Pacific a n d I n d i a n
O c e a n u p p e r layer saltinity b u d g e t , J. Phys.
Oceanogr. 14, 7 4 7 , 1984.
Reid, J . a n d R. L y n n , O n t h e influence of t h e
N o r w e g i a n - G r e e n l a n d a n d W e d d e l l Seas
u p o n t h e b o t t o m w a t e r s of t h e I n d i a n a n d
Pacific o c e a n s Deep Sea Res., 18 1 0 6 3 , 1 9 7 1 .
R o e m m i c h , D., a n d C. W u n s c h , T w o t r a n s a t ­
lantic sections: M e r i d i o n a l circulation a n d
h e a t flux in t h e s u b t r o p i c a l N o r t h Atlantic
O c e a n , Deep Sea Res., 32, 6 1 9 , 1985.
S t o m m e l , H . , a n d A. A r o n s , O n t h e abyssal
circulation of t h e w o r l d o c e a n , 1, S t a t i o n a r y
p l a n e t a r y flow p a t t e r n s o n a s p h e r e Deep
Sea Res., 6, 140, 1960.
W y r t k i , K., Physical o c e a n o g r a p h y of t h e
S o u t h e a s t Asian w a t e r s , Naga Rep., Vol. 2,
195 p p . , Univ. of Calif. San D i e g o , S c r i p p s
Inst, of O c e a n o g r . , La Jolla, Calif., 1 9 6 1 .
W y r t k i , K. Oceanographic Atlas of the Interna­
tional Indian Ocean Expedition, 531 p p , N a ­
tional Science F o u n d a t i o n , W a s h i n g t o n ,
D.C., 1 9 7 1 .
This item was contributed by A r n o l d L. G o r ­
d o n , Lamont-Doherty Geological Observatory, Pal­
isades, N.Y.
News &
Announcements
Ocean Sciences Award
P A G E 110
T h e O c e a n Sciences A w a r d is p r e s e n t e d by
t h e O c e a n Sciences Section of A G U to a n in­
dividual w h o h a s m a d e o u t s t a n d i n g a n d long­
s t a n d i n g c o n t r i b u t i o n s to t h e o c e a n sciences.
Previous recipients are
E u g e n e C. L a F o n d
R i c h a r d C. V e t t e r
R o b e r t E. Wall
F e n n a n D. J e n n i n g s
W a y n e V. B u r t
W. Stanley Wilson
C u r t i s A. Collins
1982
1983
1983
1984
1984
1984
1985
N o m i n a t i o n s a r e solicited for c a n d i d a t e s for
t h e O c e a n Sciences A w a r d in 1986. L e t t e r s of
n o m i n a t i o n s h o u l d b e s e n t to A r n o l d L. G o r ­
d o n , P r e s i d e n t - E l e c t , O c e a n Sciences Section,
L a m o n t - D o h e r t y Geological O b s e r v a t o r y , Pal­
isades, N Y 10964. T h e d e a d l i n e for n o m i n a ­
tions is May 1, 1986. N o m i n a t i o n s m a y b e ac­
c o m p a n i e d by s e c o n d i n g n o m i n a t i o n s a n d a
r e s u m e of t h e c a n d i d a t e .
Black Sea Cruise
P A G E 110
T h e National Expeditionary Planning
C o m m i t t e e of t h e U n i v e r s i t y - N a t i o n a l O c e a n ­
o g r a p h i c L a b o r a t o r y System ( U N O L S ) h a s
d e s i g n a t e d t h e R/V Knorr to s u p p o r t o c e a n o ­
g r a p h i c p r o g r a m s in t h e Black Sea d u r i n g
1987. R e s e a r c h e r s a r e invited to s u b m i t r e ­
q u e s t s for s h i p t i m e in 1987 a n d 1988 to s u p ­
p o r t projects in t h e Black Sea, t h e M e d i t e r r a ­
n e a n Sea, t h e R e d Sea, a n d t h e I n d i a n
O c e a n . P r o p o s a l s for t h e s u p p o r t of t h e sci­
entific p r o g r a m s s h o u l d b e s u b m i t t e d in ac­
c o r d a n c e with t h e f u n d i n g a g e n c y d e a d l i n e s .
R e q u e s t s for s h i p u s e s h o u l d b e s e n t s o o n
to J . D. D o n n e l l y , M a n a g e r , M a r i n e O p e r a ­
tions, W o o d s H o l e O c e a n o g r a p h i c I n s t i t u t i o n ,
Woods Hole, MA 02543 (telephone: 617-5481400, ext. 2 7 3 6 ) , o r to W. D. B a r b e e , E x e c u ­
tive S e c r e t a r y , U N O L S Office, W B - 1 5 , School
of O c e a n o g r a p h y , University of W a s h i n g t o n ,
Seattle, W A 9 8 1 9 5 ( t e l e p h o n e : 2 0 6 - 5 4 3 2283).
Meeting Report
Ocean Telemetry
Workshop
P A G E 110
An informal workshop on ocean telemetry
a n d p l a t f o r m location was h e l d o n J a n u a r y
15, 1986, d u r i n g t h e A G U O c e a n Sciences
M e e t i n g in N e w O r l e a n s , La. P l a n s for t h e
w o r k s h o p g r e w f r o m t h e realization t h a t p r e -