Organic Carbon and Carbonate as Paleoproductivity Proxies
333
600
1 2
3 4
5
6
7
8
Ia
1:
400
0
.2l 200
0..
'"
0..
0
25
~
cJ,
N
20
.,.,
:b
15
0 10
~
0..
'"
0..
50
100
150
200
250
Age lkal
(Brummer and van Eijden 1992; van Kreveld et al.
1996; Riihlemann et al. 1996):
(1) Carbonate dissolution leads to an underestimation of carbonate fluxes. Therefore, the carbonate
preservation state through time has to be checked,
for example, by investigations offoraminiferal fragmentation, or weight percentage of the coarse
fraction, or other indicators of carbonate dissolution (Le and Shackleton 1992; Howard and Prell
1994; Bickert and Wefer 1996; Riihlemann et al.
1996; Dittert et al. this VOlume).
Fig. 15. Scatter plots of organic carbon flux normalized
to 3200 m water depth (according to Suess 1980) versus
carbonate flux. (a) sediment trap data from different
productivty systems of the pelagic Atlantic and Pacific
(from van Kreveld et al. 1996 based on literature data).
(b) sediment trap data from the pelagic western equatorial Atlantic (Fischer and Wefer 1995 and unpubl data).
Organic carbon flux rates obtained from various water
depths were normalized to 3200 m to account for the
decomposition and related decrease of organic carbon
with depth. For normalization the equation of Suess
(1980) can be used or any other equation describing the
decrease of particulate C". flux with depth (see Bishop
1989 for review).
300
9 10 11
Fig. 14. Comparison of paleoproductivities estimated from ora
ganic carbon between the eastern
and western tropical Atlantic. (a)
Paleoproductivities of cores GeoB
1016-3 and 1523-1 after Miiller and
Suess (1979). (b) Ratio of paleoproductivities (1016-3 /1523-1);
b
stippled line marks the Holocene
(0-6 ka) ratio. Estimates are based
on average sedimentation rates
(4 cm· j ka for GeoB 1016-3 and
2 cm· j ka for GeoB 1523-1), data
of core GeoB 1016-3 are from
Schneider et al. (1995).
350
400
o
50
100
150
200
15~~~~~~~-L~~~~~~-r
>ro
-0
~E
o Ol
oS
.s::
0.
Q)
-0
ID
~
E
o
o
N
'"
10
5
o
C5 10
x
::>
"i'
~
o
U
o
F Corg = 0 .
043 * F CaC0 3 + 0.35
n=313, r=O.77
a
a
a
co
a
a
a
F Corg = 0 .
033 * F c aco 3 + 0.16
n = 113, r= 0.78
a
b
50
100
150
200
Carbonate flux [mgCaC0 3 m· 2 day" ]
333
600
1 2
3 4
5
6
7
8
Ia
1:
400
0
.2l 200
0..
'"
0..
0
25
~
cJ,
N
20
.,.,
:b
15
0 10
~
0..
'"
0..
50
100
150
200
250
Age lkal
(Brummer and van Eijden 1992; van Kreveld et al.
1996; Riihlemann et al. 1996):
(1) Carbonate dissolution leads to an underestimation of carbonate fluxes. Therefore, the carbonate
preservation state through time has to be checked,
for example, by investigations offoraminiferal fragmentation, or weight percentage of the coarse
fraction, or other indicators of carbonate dissolution (Le and Shackleton 1992; Howard and Prell
1994; Bickert and Wefer 1996; Riihlemann et al.
1996; Dittert et al. this VOlume).
Fig. 15. Scatter plots of organic carbon flux normalized
to 3200 m water depth (according to Suess 1980) versus
carbonate flux. (a) sediment trap data from different
productivty systems of the pelagic Atlantic and Pacific
(from van Kreveld et al. 1996 based on literature data).
(b) sediment trap data from the pelagic western equatorial Atlantic (Fischer and Wefer 1995 and unpubl data).
Organic carbon flux rates obtained from various water
depths were normalized to 3200 m to account for the
decomposition and related decrease of organic carbon
with depth. For normalization the equation of Suess
(1980) can be used or any other equation describing the
decrease of particulate C". flux with depth (see Bishop
1989 for review).
300
9 10 11
Fig. 14. Comparison of paleoproductivities estimated from ora
ganic carbon between the eastern
and western tropical Atlantic. (a)
Paleoproductivities of cores GeoB
1016-3 and 1523-1 after Miiller and
Suess (1979). (b) Ratio of paleoproductivities (1016-3 /1523-1);
b
stippled line marks the Holocene
(0-6 ka) ratio. Estimates are based
on average sedimentation rates
(4 cm· j ka for GeoB 1016-3 and
2 cm· j ka for GeoB 1523-1), data
of core GeoB 1016-3 are from
Schneider et al. (1995).
350
400
o
50
100
150
200
15~~~~~~~-L~~~~~~-r
>ro
-0
~E
o Ol
oS
.s::
0.
Q)
-0
ID
~
E
o
o
N
'"
10
5
o
C5 10
x
::>
"i'
~
o
U
o
F Corg = 0 .
043 * F CaC0 3 + 0.35
n=313, r=O.77
a
a
a
co
a
a
a
F Corg = 0 .
033 * F c aco 3 + 0.16
n = 113, r= 0.78
a
b
50
100
150
200
Carbonate flux [mgCaC0 3 m· 2 day" ]