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320
310
300
290
C S
280
C S
270
260
250
+15 C temperature increase
relative to 1 x CO 2 SSTs
+8 C temperature increase
relative to 1 x CO 2 SSTs
240
90
N
45
N
N
Latitude
0
45
S
90
S
Figure 20.2 Zonal mean sea-surface temperatures (SSTs) as a function of CO 2
levels and latitude. KS2005 denotes simulations from Kiehl and Shields ( 2005 ).
CCSM3 runs were completed with Community Climate System Model 3;
CCSM4 runs were completed with Community Climate System Model 4. Based
on oxygen isotope records from conodonts, Joachimski et al .( 2012 ) report a
þ
8 Cwarming of low-latitude sea-surface temperatures across the Permian
Triassic
-
15 C warming of low-latitude sea-surface
temperatures from the middle Permian up to the Middle Triassic. For reference,
both potential temperature increases are shown here, relative to a simulation
of Permian climate with 1
boundary; Sun et al .( 2012 )reporta
þ
present-day CO 2 (355 ppm). Temperatures below
1.8 C (271.3 K) correspond to sea-ice.
-
increase in CO 2 leads to a zonally averaged low-latitude sea-surface temperature
increase that is highly consistent with the
þ
8 ˚ C warming reported by Joachimski
et al .( 2012 ).
A
þ
15 ˚ C warming of the equatorial sea surface (Sun et al ., 2012 ) is more
dif
cult to achieve, and exceeds the temperature increase associated with a ten-fold
increase in CO 2 to 3550 ppm (Kiehl and Shields, 2005 ). Based on a survey of
climate models, an approximately 2 - 4 C global temperature increase is expected
for each doubling of CO 2 (Rohling et al ., 2012 ). The magnitude of the long-term
warming reported by Sun et al .( 2012 ) thus requires higher climate sensitivity,
extreme CO 2 levels or large quantities of other greenhouse gases (such as CH 4 )in
addition to CO 2 .
20.6 Global cooling
Stratospheric volcanic emissions of short-lived sulfur gas could produce transient
aerosol-induced cold spells within a long-term greenhouse warming trend from
longer-lived CO 2 . The eruption of the Siberian Traps occurred at relatively high
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