2.1. RADIATIVE FORCING|
2.2.A. Carbon Budget
2.2.B. Atmospheric Carbon Dioxide
2.2.C. Recent Anomalies in the Global Carbon Cycle
2.2.D. Carbon Doxide Record Over the Last Climatic Cycle
2.2.E. Carbon Dioxide Concentrations in the Future
2.4. NITROUS OXIDE
2.1. Radiative Forcing
In an unperturbed state, the net incoming solar radiation at the top
of the atmosphere (Sn) must be balanced by the
outgoing longwave radiation (Lo), on an annual basis globally.
While this may not be exactly so in any given year, but when a long
time series of the annual differences are viewed, Sn must equal Lo.
A true change in either Sn or Lo is called Radiative Forcing.
A positive radiative forcing, that is, when Lo is less than Sn,
results in warming of the Earth surface. And, vice versa.
Human activities can result in changes of the various components of
the climate system, the climatic effects of which can be estimated
by investigating the magnitude of radiative forcing. Estimates of the
globally averaged radiative forcing due to changes
in greenhouse gases and aerosols from pre-industrial time to the
present, and changes in solar variability from 1850 to the present
are shown in
The height of the bar indicates a mid-range estimate of the forcing,
whilst the lines above show the possible range of values. An
indication of the relative confidence in the estimate is given
below each bar.
The increase in CO2 concentration from 280 ppmv (preindustrial)
to 360 ppmv (1995) resulted in a positive radiative forcing of the
climatic system of about 1.5 W/m2. A further 0.5 W/m2 forcing
has resulted from increase in methane concentration (700 ppbv
preindustrial to 1700 ppbv in 1995). The total radiative forcing
due to greenhouse gases is thus estimated to be about 2.5 W/m2.
A general rule of thumb is warming of about 0.6 C results from
1 W/m2 forcing of the present climate system.
The negative values for aerosols
should not necessarily be seen as an offset against the greenhouse gas
forcing because of uncertainities over the applicability of global mean
radiative forcing in the case of non-homogeneously distributed species
such as aerosols and ozone. It is especially important to note the
confidence level associated with tropospheric aersol indirect effects.
A summary of key greenhouse gases affected by human activities is shown
below in Table 2.1. From this table and Figure 2.1, you can note that
the concentration of CO2 increased by about 80 ppmv since the preindustrial
times and the resulting radiative forcing is about 1.5 W/m2. But, during
the same period, the concentration of methane increased by about 1 ppmv,
but the consequent radiative forcing is 0.5 W/m2, which clearly shows
that methane is a much more powerful greenhouse gas than CO2. It is also
important to note the lifetimes given for each of the gases. Note that
the growth rates are for the decade of 1980s.
Climate forcings in the industrial era
Solar variability, ozone and climate
Table 2.1: A Summary of Key Greenhouse Gases Affected by Human Activities
Carbon Dioxide CO2
Nitrous Oxide (N2O)
Chloro-Flouro Carbon (CFC-12)
Recent rate of
change per year
ppmv: parts per million by volume
ppbv: parts per billion by volume
pptv: parts per trillion by volume
No single lifetime for carbon dioxide can be defined because of the different rates of uptake by various sinks.
2.2.A. Carbon Budget
The global carbon budget is shown schematically in
Our understanding of the global carbon cycle has improved
considerably in the recent years, particularly in how the carbon
from the atmosphere is removed and stored in sinks on land and
ocean. However, considerable uncertainity exists regarding the
processes which contribute to the sinks on land.
The main anthropogenic sources of carbon dioxide are the
burning of fossil fuels (with additional contributions
from cement production), and land-use changes.
During the 1980s, the average emissions from fossil fuel burning
and cement production were 5.5 +/- 0.5 GtC/yr. A GtC is a
Giga Tonne of Carbon or 10^9 (billion) tonnes of
carbon or 10^15 (Peta) grams of carbon.
Land-use changes cause both release and uptake of CO2.
On average CO2 will be released to the atmosphere if
the original ecosystem stored more carbon than the modified
ecosystem which replaces it. Thus, deforestation acts as a
During the 1980s, tropical deforestation is estimated to have
resulted in an average emission to the atmosphere of 1.6 +/-
1.0 GtC/yr. However, in the mid- and high-latitudes there are
areas where forests are regrowing after clearing in the past,
and where sequestration of carbon is currently occurring; a sink
of about 0.5 +/- 0.5GtC/yr is estimated.
Thus, the latest estimate of net CO2 release due to
global land-use changes is 1.1 +/- 1.2 GtC/yr.
Carbon exchanges between vegetation on land and the atmosphere
are considerable, at annual scales. Global vegetation fixes about
100-120 GtC/yr through the process of photosynthesis (gross
primary production). About 40-50% of this carbon is respired
by the vegetation (autotrophic respiration) , with the
result net primary production of global vegetation is
about 61.4 GtC/yr. Heterotrophs in the soil constribute a similar
amout to the atmosphere, or about 60 GtC/yr (heterotrophic
or soil respiration).
Thus, the current estimate for carbon sink on land is about
There are also considerable exchanges of CO2 between
the atmosphere and the oceans, of the order of about 90 GtC/yr,
with a net sink of about 2 GtC/yr.
Carbon in the surface ocean layers is used by the marine biota,
and more is exchanged with the intermediate to deep layers in the
ocean. The carbon stocks in the ocean are significantly larger
than on land (cf. Figure2.2 ).
The carbon budget for the period 1980-1990 is shown below in Table 2.2
About the Carbon Cycle
Oh where oh where does the co2 go?
Table 2.2: Annual average anthropogenic carbon budget for 1980 to 1990. Units are GtC/yr.
| CO2 Sources || |
| || |
|(1) Emissions from fossil fuels and cement production|| 5.5 +/- 0.5|
|(2) Net emissions from changes in tropical land-use|| 1.6 +/- 1.0|
|(3) Total anthropogenic emissions = (1)+(2)|| 7.1 +/- 1.1|
| || |
| Partitioning amongst reservoirs || |
| || |
|(4) Storage in the atmosphere|| 3.2 +/- 0.2|
|(5) Ocean uptake|| 2.0 +/- 0.8|
|(6) Uptake by Northern Hemisphere forest regrowth|| 0.5 +/- 0.5|
|(7) Additional terrestrial sinks (CO2 fertilisation, Nitrogen fertilisation, || |
|climatic effects) = [(1)+(2)]-[(4)+(5)+(6)] || 1.4 +/- 1.5|
Biomass Burning and CO2
2.2.B. Atmospheric Carbon Dioxide
Accurate and direct measurements of the concentration of
CO2 in the atmosphere began in 1957 at the South
Pole and in 1958 at Mauna Loa, Hawaii. The Mauna Loa record
is shown below in Figure2.3.
In 1958, the concentration of CO2 was about 315 ppmv,
and the growth rate was about 0.6 ppmv/yr. This growth rate has
generally been increasing since then; it averaged 0.83 ppmv/yr
in the 1960s, 1.28 ppmv/yr during the 1970s, amd 1.53 ppmv/yr
during the 1980s. In 1994, the concentration of CO2
at Mauna Loa was 358 ppmv. The concentration in April of 2000 was a little
over 370 ppmv, the most recent month for the which the data were available.
Data from Mauna Loa are close to,
but are not precisely the global mean value. The Mauna Loa record
is due to Prof. Keeling of the Scripps Institution of Oceanography.
The annual cycle in the Mauna Loa record (Figure 2.3)
is due to the seasonality of vegetation. In early spring, the
concentration of CO2 is at its maximum, and as the
plants greenup, the concentration drops, reaching a minimum value
towards the end of the summer, and when it starts to build up
again. This swing in the amplitude is most pronounced in the
records from the northern high latitudes, where it can be as large
as 15 ppmv.
The atmospheric CO2 record prior to 1957 comes mainly
from air bubbles in ice cores, which is reasonably accurate
(Figure 2.4). This
record extends back almost a 1000 years. Data from the period before
that is of poor quality because of the defects in the ice.
Over the last 1000 years, CO2 concentration in the
atmosphere has fluctuated at about +/- 10 ppmv around 280 ppmv.
Therefore, the 20th century increase in CO2
concentration is unparalleled in the past 1000 years.
There are at least three arguments to be made for the case that
the observed increase in atmospheric CO2 concentration
is due to emissions related to human activity.
- The rise in atmospheric CO2 concentration closely
follows the increase in emissions related to fossil fuel burning
and cement production.
- The inter-hemispheric gradient in atmospheric CO2
concentration is growing in parallel with CO2 emissions
(Figure 2.5). That is, there is more land mass
in the Northern hemisphere, and therefore more human activity,
and thus, higher emissions, which is reflected in the CO2
growth in the Northern hemisphere (compared to the SH).
- Fossil fuels and biospheric carbon are low in Carbon 13 (an isotope).
The ratio of carbon 13 to carbon 12 in the atmosphere has been decreasing.
2.2.C. Recent Anomalies in the Global Carbon Cycle
The early 1980s were characterized by a period of relatively constant
or slightly declining fossil carbon emissions. After 1985, carbon
emissions exceeded the 1979 level. With the collapse of the former
Soviet Union in the early 1990s, emissions decreased again.
Direct measurements and ice core data have revealed a general
decrease in atmospheric levels of Carbon 13 relative to Carbon 12
by about 1% over the last century. This decrease is expected from
the addition of fossil and/or biospheric carbon, both of which are
low in Carbon 13 relative to the atmosphere. The atmospheric record
of Carbon 13 shows a decrease of about 0.4% between the first
measurements in 1978 and early 1990s.
Relative to the long-term average rate of atmospheric rate of
CO2 concentration increase (about 1.5 ppmv/yr), the
years 1988 to 1989 had relatively high CO2 growth
rates (about 2.0 ppmv/yr), while subsequent years (1991 to 1992)
had very low growth rates (about 0.5 ppmv/yr). The growth rate
has since rebounded in the mid-1990s.
The CO2 record exhibits a seasonal cycle, with small
peak-to-trough amplitude (about 1 ppmv) in the Southern Hemisphere,
but increasing northward to about 15 ppmv in the boreal forest
zone (55-65 degrees North). This cycle is caused by the seasonal
uptake of atmospheric CO2 by terrestrial ecosystems.
At Mauna Loa, the amplitude was roughly constant at 5.2 ppmv
from the begining of the record, until the mid 1970s. It then
increased from the late 1970s to about 5.8 ppmv for most of the
1980s. The recent data indicate a further increase. This variation
clearly indicates a change in terrestrial vegetation activities.
Recently, an increase in amplitude of the seasonal cycle of
atmospheric carbon dioxide exceeding 20% since the early 1970s,
and an advance in the timing of the drawdown of CO2
in spring and early summer of up to 7 days has been reported.
This suggests that plants in the northern high latitudes have been
growing vigorously, and that springtime greening is happening
earlier. This has also been confirmed with analysis of satellite
data for the 1980s.
Increased Plant Growth in the North
Current Data as Figures (CMDL)
2.2.D. CO2 Record Over the Last Climatic Cycle
The close association between CO2 and temperature
changes during the last climatic cycle was revealed by data
from the ice core record (Figure 2.6).
Samples from Greenland and Antarctica representing the last glacial
maximum (about 18,000 years before present or 18K BP), indicate
that CO2 concentration at that time was about 190-200
ppmv, that is, about 70% of the pre-industrial level.
Thus, an increase of about 80 ppmv occurred in parallel
with the warming at the end of the glacial period, when the
estimated rise in mean surface temperature of the Earth was about
4C over about 10,000 years. The Antarctic record
shows a marked correlation between temperature and
CO2 and CH4 concentration.
The Antarctic record provides an important perspective for recent
and potential future changes, although the magnitudes and rates of
changes in the paleo record may differ from those due to greenhouse
The Latest Figure
2.2.E. CO2 Concentrations in the Future
In order to predict future concentrations of CO2 in
the atmosphere, an understanding of the relationship, and its
quantification, between emissions and concentrations is required.
Models have been used towards this purpose, and these do have well
recognised limitations, for example, they do not include the
climatic feedback on the CO2 cycle.
Two important questions are considered here -
- For a given CO2 emission scenario, how might
CO2 concentrations change in the future?
- For a given CO2 concentration profile leading to
stabilization of the level of concentration, what anthropogenic
emissions are implied?
For this purpose, certain standard emission scenarios have been developed by the
Intergovernmental Panel on Climate Change (IPCC) in 1992; these are called IS92a, b, c, d, e, and f
- IS92a is the so-called business-as-usual scenario, that is,
emissions continue to grow at the present rate.
- IS92c represents the lower-end scenario of
emissions, with the assumption of low population growth, low
economic growth, and constraints on fossil fuel supplies.
- IS92e represents the higher-end scenario of
emissions, with the assumption of moderate population growth,
high economic growth, high fossil fuel availability and phase-out of nuclear power.
Now, we consider the first question, that is, for a given CO2 emission scenario, how might CO2
concentrations in the future might change? Model results are shown
in Figure 2.7b.
- All scenarios indicate increases in concentrations well above
pre-industrial levels by the year 2100 (75 to 220% higher).
- None of the scenarios show a stabilization of concentration before
the year 2100, that is, the concentration in the atmosphere tends
to keep increasing.
- IS92a, IS92b, IS92e and IS92f all produce a doubling of the
preindustrial concentration before 2070 with rapid rates of
concentration growth. However, neither IS92c nor IS92d results in
doubled preindustrial concentration by 2100.
- Stabilization of current global emissions of CO2
does not lead to stabilization of CO2 concentrations by
the year 2100 (Figure 2.7c).
The concentration may reach about 500 ppmv by the end of the 21st
century, and continues to increase slowly for several hundred years.
Let us now consider the second question, that is, for a given
CO2 concentration profile leading to stabilization,
what anthropogenic emissions are implied? Towards this purpose,
concentration profiles have been devised leading to stabilization
from 350 ppmv to 750 ppmv; for comparision, the preindustrial
concentration was about 280 ppmv and 1993 concentration was
356 ppmv. These profiles are shown in Figure 2.8a.
These profiles have been devised such that stabilization at
350, 450, 550, 650 and 750 ppmv is achieved in 2150, 2100,
2150, 2175, 2250, respectively. The selection of the range 350 to 750 ppmv is quite arbitrary and
has no policy implications. These profiles are illustrative and
give a smooth transistion from the present levels to the levels of
stabilization. The model derived profiles of total anthropogenic emissions from
fossil fuel burning, changes in land-use and cement production,
are shown in Figure 2.8b.
- Stabilization at any level of concentration studied, from 350 to
750 ppmv, is possible only if emissions are reduced well
below 1990 levels.
- Emissions for all stabilization levels are lower
than those for IS92a (business-as-usual
scenario) and, of course, IS92e (the highest
emission scenario), even in the first few decades of the 21st century.
- Emissions for the IS92c (the lowest emissions
scenario) lie between the emissions which in this study lead to
stabilization between 450 and 550 ppmv.
- Stablization at a certain level can also achieved following profiles
other than those shown in Figure 2.8a.
But, to a first approximation, the amount of total carbon emitted is insensitive to the
atmospheric CO2 concentration profile. Therefore, it
is illustrative to look at the actual amount of carbon emitted (Table 2.3).
Table 2.3: Emissions of carbon accumulated from 1990 to 2100
leading to stabilization of CO2 concentration at 350, 450, 550, 650, and 750 ppmv.
| ||Accumulated Emissions from 1990 to 2100 (GtC)|
| IS92 Emission Scenarios || |
| IS92b|| 1430|
| IS92c|| 770|
| Stabilization Case || |
Stabilization of CO2 at or below 750 ppmv (the highest
level studied) would require accumulated emissions from 1900 to
2100 lower than those occurring under IS92a,
IS92b, IS92e and IS92f scenarios, and even lower in
the next two centuries.
In order to achieve stabilization at 350 ppmv (the lowest level),
even the lowest emission scenario IS92c leads
to emissions well above 300-430 GtC required.
The previously shown model results on future CO2
emissions and atmospheric concentrations did not take into
account any feedbacks on the carbon cycle, especially those
related to global vegetation. Higher temperatures and increased
precipitation, thought to result from the greenhouse effect, can
increase photosynthesis and plant growth, and hence, carbon
storage in vegetation and litter (a negative feedback). Also,
experiments have shown that plants grown in CO2
rich air tend to grow more vigorously, as CO2 is a
nutrient (the fertilization effect).
The storage of carbon in the soils tends to decrease with
warming due to increased rates of decomposition (a positive
feedback). On the otherhand, soils which are flooded tend to
store large amounts of carbon in the form of peat. In anycase, it is
illustrative to see how one such feedback
can alter the previously reported results on emission and
Figure 2.9 shows modifications to the
business-as-usual scenario (IS92a) at different
rates of vegetation net primary productivity (NPP) enhancement.
Indeed some reasonably significant changes in atmospheric
CO2 can occur depending on the NPP enhancement factor
(about 14 percent or about 50-100 ppmv in 110 years or so).
However, it is also abundantly clear that vegetation
growth enhancement cannot be assumed to
offset anthropogenic carbon emissions.
Forty percent NPP enhancement has been observed in some plants,
under closed chamber and optimal water and nutrient situations.
In general, there is no reason to believe that this can achieved
globally under all conditions, and the real number may be atleast
half of this or even less.
About IPCC Emission Scenarios
Role of CO2 in Global Warming
Methane (CH4) is another naturally occuring greenhouse
gas whose concentration in the atmosphere has been increasing as a
result of human activities (rice paddies, animal husbandry,
landfills, biomass burning, and fossil fuel production and use).
Ice core measurements of methane concentration indicate that its
concentration has increased from a preindustrial level of about
750 ppbv to over 1700 ppbv in early 1990s (Figure 2.10).
Globally methane increased by about 7% over the decade from 1983.
However, the decade of 1980s were characterized by declining
methane growth rates, dropping from about 16 ppbv/yr in 1980
to about 10 ppbv/yr by 1990. Growth rates slowed dramatically in
1991 and 1992. This is variously ascribed to declining fossil fuel
use, decreased biomass burning and the drop in global temperatures
due to Mount Pinatubo eruption in mid-1991. Since then, however,
growth rates have rebounded (Figure 2.11).
Note that although methane concentration is in ppbv, compared to
carbon dioxide, it is a highly effective radiative gas.
The increase in methane since preindustrial times is estimated to
have resulted in a radiative forcing of about 0.5
W/m2, which is quite significant when compared to the
increase in carbon dioxide concentration during the same time
period and its radiative forcing (1.5 Watts/m2)
Analysis of the global methane budget indicate that about 20%
of the total annual methane emissions are related to fossil fuel
use (for example, combustion, coal mines, natural gas production,
petroleum industry operations, etc). In total, it has been estimated that
about 60-80% of current methane emissions are due to anthropogenic activities.
About 20% of current methane emissions are related to natural
sources such as wetlands, termites, oceans etc.
Climate change can either -
Thus, global warming can either increase or decrease natural methane
production depending on the extent to which the temperature increase
is matched by increased precipitation.
- increase methane flux due to northward spread of
peat-forming areas from increased precipitation in the high
- decrease from drying out and/or permafrost melting
leading to loss of peat-forming areas in the continental
Learn more about methane
Methane growth slows
2.4. Nitrous Oxide
There are many sources of Nitrous Oxide (N2O), both
natural and anthropogenic, which are difficult to identify and
quantify. The main anthropogenic sources are from agriculture,
biomass burning and industrial processes. The
best estimate of 1980s anthropogenic emission of N2O
is 3 to 8 TgN/yr (terra grams of Nitrogen or 10^12
grams of Nitrogen). Natural sources are probably twice
as large as anthropogenic sources.
Ice core measurements of nitrous oxide concentration indicate that
its concentration has increased from a preindustrial level of about
275 ppbv to over 310 ppbv in early 1990s (Figure 2.12).
The average growth rate over the past four decades was about
0.25%/yr (0.8 ppbv/yr). The radiative forcing due to change in
nitrous oxide concentration from preindustrial level to the present
has been estimated at about 0.14 W/m2 (Figure 2.12).
Because of its long life-time, about 120 years, if emissions were
held constant at the present level, atmospheric N2O
abundance would still climb from 311 ppbv to about 400 ppbv over
the next several hundred years.
Learn more about N2O
Aerosols are suspensions of particles in the atmosphere, with
diameters in the range 10-3 to 10^-6 meters.
Tropospheric aerosols are formed by -
The release of sulphur dioxide from fossil fuel combustion and
biomass burning, are the main anthropogenic sources of aerosols.
- dispersal of material from the surface, for example dust,
- direct emission of material into the atmosphere, for example, smoke,
- chemical reactions in the atmosphere which convert gases, such as
sulphur dioxide, into particles.
The addition of tropospheric aerosols from anthropogenic sources
can influence the radiative balance in two major ways -
- through absorption and scattering of solar radiation back into
the outer space, and is known as the direct effect,
- by acting as nuclei on which cloud droplets form; aerosols can
thus influence the formation, lifetime and radiative properties
of clouds, which is known as the indirect effect.
There are many uncertainities associated with how aerosols influence
the climate. Aerosols are highly variable spatially, both in their
concentration and chemical composition, and direct observations of
their amount and kind are begining to emerge just now. Nevertheless, some
attempts have been to estimate the globally averaged radiative
forcing due to aerosols from anthropogenic sources. The direct radiative
forcing due to increases in sulphate aerosol
since 1850, averaged globally, is estimated to lie between
-0.25 to -0.9 W/m2. And, the direct effect of aerosol from biomass burning
is estimated to be in the range of -0.05 to -0.6 W/m^2.
The spatial distribution of direct radiative forcing due to sulphate
aerosols derived from a radiative transfer model is shown in
Figure 2.13. The largest forcing occurs over
or close to industrial activity. Over the eastern USA, central
Europe, and eastern China, sulphate forcing may have offset much
of, or in places been greater than, the greenhouse gas forcing.
However, it must be remembered than local forcing does not
necessarily govern local response, for changes can still happen
locally due to circulation as the atmosphere may respond to forcings
Aerosols and climate
Balancing the Carbon Budget ...
Carbon Dioxide Information Analysis Center
US Emissions of Greenhouse Gases
The Carbon Cycle, Climate ...
GG 312 Fall 2000 Home Page
27 Nov 2000