The data selection method has been described in Thoning et al., J. Geophys. Research, (1989) vol. 94, 8549-8565. Different data selection methods are compared in that paper, including no selection. The methods give annual means differing by a few tenths of 1 ppm . I assume that you have read the README file [ 4 ] when downloading the data. The hourly means are NOT pre-processed, but they are flagged when the st.dev. of the minute averages is large.



The good, the bad and the ugly stations.



Diekirch (Luxemburg) CO2 measurements compared to wind speed

Graph from [

Diekirch (Luxemburg) CO2 measurements compared to wind speedGraph from [ 6 ].

3. Variations of CO2 due to the seasons:



Monthly trends 2002-2004 of 2 NH stations (Barrow and Mauna Loa) and 2 SH stations (Samoa and South Pole)



As can be noticed, the variation at Mauna Loa is smaller than at Barrow and the SH stations have a much smaller seasonal influence than the NH stations. Also, although the trend of the SH stations is near the same, there is some lag between the NH and SH stations. This is the first indication that the source of the increase is situated in the NH, as the ITCZ (intertropical convergence zone) forms a barrier for the exchange of CO2 (and aerosols) between the NH and the SZ. This is even more clear in the longer term yearly trends:





Trends in yearly averages of CO2 levels at different stations.



The trend of the SH stations has a growing delay of 6-12 months behind the NH trend. But all yearly average data of the "best" stations (and the average of least contaminated data from less suitable stations like Schauinsland) are within 5 ppmv for similar growth.





The trend of the SH stations has a growing delay of 6-12 months behind the NH trend. But all yearly average data of the "best" stations (and the average of least contaminated data from less suitable stations like Schauinsland) are within 5 ppmv for similar growth. Trends in yearly averages of CO2 levels at different stations. As can be noticed, the variation at Mauna Loa is smaller than at Barrow and the SH stations have a much smaller seasonal influence than the NH stations. Also, although the trend of the SH stations is near the same, there is some lag between the NH and SH stations. This is the first indication that the source of the increase is situated in the NH, as the ITCZ (intertropical convergence zone) forms a barrier for the exchange of CO2 (and aerosols) between the NH and the SZ. This is even more clear in the longer term yearly trends: Monthly trends 2002-2004 of 2 NH stations (Barrow and Mauna Loa) and 2 SH stations (Samoa and South Pole)

4. Where to measure? The concept of "background" CO2 levels.



Figure 3.1 Diurnal variation in the concentration and carbon isotopic ratio of atmospheric

CO 2 in a coastal redwood forest of California, 18-19 May 1955, Big Sur St. Pk.

(Keeling, 1958. Reproduced by permission of Pergamon Press.)



Several others measured CO2 levels/d13C ratios of the their own samples too. This happened at several places in Germany (Heidelberg, Schauinsland, Nord Rhine Westphalia). This confirmed that local production was the origin of the high CO2 levels. The smallest CO2/d13C variations were found in mountain ranges, deserts and near the oceans. The largest in forests, urban neighbourhoods and non-urban, but heavely industrialised neighbourhoods. When the reciproke of CO2 levels were plotted against d13C ratios, this showed a clear relationship between the two. Again from [



Figure 3.5 Relation between carbon isotope ratio and concentration of atmospheric CO 2 in

different air types from measurements summarized in Table 3.4

(Keeling, 1958, 1961: full squares; Esser, 1975: open circles; Freyer and Wiesberg, 1975,

Freyer, 1978c: open squares). All 13C measurements have not been corrected

for N 2 O contamination (Craig and Keeling, 1963), which is at the most in the area of + 0.6‰



The search for background places.

Keeling then sought for places on earth not (or not much) influenced by local production/uptake, thus far from forests, agriculture and/or urbanisation. He had the opportunity to launch two continuous measurements: at Mauna Loa and at the South Pole. Later, other basic stations were added, all together 10 from near the North Pole (Alert, NWT, Canada) to the South Pole, most of them working continuous, some working with regular flask sampling.



We are interested in CO2 levels in a certain year all over the globe and the trends of the CO2 levels over the years. So, here we are at the definition of the "background" level:

Yearly average data taken from places minimal influenced by vegetation and human sources are deemed "background".

For convenience, the yearly average data from Mauna Loa are used as reference. One could use any base station as reference or the average of the stations, but as all base stations (and a lot of other stations, even Schauinsland) are within 5 ppmv of Mauna Loa, with near identical trends, and that station has the longest near-continuous CO2 record, Mauna Loa is the reference.



Figure 3.5 Relation between carbon isotope ratio and concentration of atmospheric COindifferent air types from measurements summarized in Table 3.4(Keeling, 1958, 1961: full squares; Esser, 1975: open circles; Freyer and Wiesberg, 1975,Freyer, 1978c: open squares). AllC measurements have not been correctedfor NO contamination (Craig and Keeling, 1963), which is at the most in the area of + 0.6‰ Several others measured CO2 levels/d13C ratios of the their own samples too. This happened at several places in Germany (Heidelberg, Schauinsland, Nord Rhine Westphalia). This confirmed that local production was the origin of the high CO2 levels. The smallest CO2/d13C variations were found in mountain ranges, deserts and near the oceans. The largest in forests, urban neighbourhoods and non-urban, but heavely industrialised neighbourhoods. When the reciproke of CO2 levels were plotted against d13C ratios, this showed a clear relationship between the two. Again from [ 7 ]: Diurnal variation in the concentration and carbon isotopic ratio of atmosphericCOin a coastal redwood forest of California, 18-19 May 1955, Big Sur St. Pk.(Keeling, 1958. Reproduced by permission of Pergamon Press.)

Measurements above the inversion layer.



Figure 3:2 Amplitude and phase shift of seasonal variations in atmospheric CO 2

at different altitudes, calculated from direct observations by harmonic analysis

(Bolin and Bischof, 1970. Reproduced by permission of the Swedish Geophysical Society.)



From [



Modern flight measurements in Colorado, CO2 levels below the inversion layer

in forested valleys and above the inversion layer at different altitudes



Modern flight measurements in Colorado, CO2 levels below the inversion layerin forested valleys and above the inversion layer at different altitudes From [ 10 ]: Amplitude and phase shift of seasonal variations in atmospheric COat different altitudes, calculated from direct observations by harmonic analysis(Bolin and Bischof, 1970. Reproduced by permission of the Swedish Geophysical Society.)

Background CO2 levels can be found over all oceans and over land at 1000 m and higher altitudes

5. Evidence of human influence on the increase of CO2 in the atmosphere.



6. References

This shows that with upslope winds, the data is influenced by local CO2 depleted air. These data are rightfully discarded from the daily/monthly/yearly averages, as they don't reflect the background CO2 levels, which we are interested in.Does discarding of "contaminated" data influence the trend over a year or several years? I have asked that question to Pieter Tans, responsible for dataprocessing of the Mauna Loa data. His answer:Several stations are deemed "good", as these have minimal influence from local vegetation and/or human emissions (traffic, heating). These are stations in the middle of the oceans, sometimes at coastal points (as long as the wind is not blowing from land side) and/or above the inversion layer. These stations, after discarding outliers, differ from each other within 5 ppmv for yearly averages, of which most is from the delay between the NH and the SH, see next item. 10 of them, spanning the globe from near the North Pole (Alert, Canada) to the South Pole, are used as reference for daily, monthly and yearly averages and yearly trends. The graphs and the data can be found at [ 5 ].Some inland stations, like Schauinsland only give reliable "background" CO2 levels, when the station (at 1200 m altitude) is above the inversion layer and with enough wind speed. This happens only about 10% of the time.And last, but not least, many inland stations are practically unsuitable for background CO2 measurement, because of incomplete mixing with the higher air layers, partly due to too many local sources/sinks like vegetation and/or human use of fossil fuels, partly due to a shielded location. This is the case for e.g. Diekirch (Luxemburg) [ 6 ], where the station is in a valley with forests, urbanisation and traffic in the main upwind direction:As can be seen, even at inconvenient places with lots of local sources/sinks, there is an inverse correlation between CO2 levels and wind speed. With higher wind speeds, CO2 levels are better mixed with higher air layers which have "background" CO2 content. This reduces the CO2 content at ground level. The assymptote of CO2 levels at high speed winds (as was seen during storm Franz, 11 January 2007) is about 385 ppmv, very close to the 382 ppmv level found at Mauna Loa in the same period. The same is true for diurnal variance: at daytime and with high enough wind speed (> 1 m/s), CO2 levels are lower and near background, while at night under the inversion layer, CO2 levels are up to 100 ppmv higher.There are two main natural influences on the CO2 levels of the atmosphere: the temperature of the ocean's surface waters and the uptake of CO2 by plants in spring/summer and the release of CO2 by the decay of dead plant material in fall/winter. This is most clear in the NH (Northern Hemisphere), where most of vegetation on land is situated.CO2 is continuously emitted by deep sea upwelling, especially in the tropics, where temperatures are high and the partial pressure of CO2 (pCO2) in the upper oceans is higher than in the atmosphere above it. CO2 is continuously absorbed in the upper ocean layers at higher latitudes, where the colder temperatures reduce the pCO2 of the oceans, lower than the pCO2 of the atmosphere. This is especially the case at the sink places of the THC (thermohaline circulation) in the Nordic Atlantic ocean. Colder water can retain more CO2 than warmer water, but in the case of CO2 there are also a lot of chemical and biological reactions which influence the solubility of CO2 and hence pCO2 at the surface of the oceans. For more details on this, Wiki has a quite good explanation.The CO2 flow between the tropics and the colder places in the oceans is relatively constant (more about that later), and doesn't influence the seasonal variation that much. More variation is in the temperature (and thus pCO2) of the mid-latitudes, where there is absorption of CO2 in winter and release of CO2 in summer. The CO2 flow of vegetation (including algues in the upper oceans) is in opposite direction: more release in winter and more uptake in summer. The net effect in the NH is a variation of +/-4 ppmv in Mauna Loa (mid Pacific Ocean, middle troposphere) between summer and winter, up to +/-20 ppmv for Barrow (Alaska, USA, sea level, near tundra) or even 35 ppmv at Schauinsland (Germany, 1200 m high). The data of Schauinsland are heavily contaminated by the nearby fully inhabited and industrialised Rhine valley. And influenced by vegetation, in this case the Black Forest of SW Germany. Only at night, when separated from the valleys by an inversion layer, and with sufficient wind speed, the CO2 levels are better mixed with the rest of the troposphere and retained. This is the case for only 10% of the data.Data series from the SH (Southern Hemisphere) show much less seasonal variation, because of the much smaller area of land/vegetation. The smallest influence of the seasons is found at the South Pole.Here follows some comparison of the Mauna Loa (selected) monthly averages with these of other stations:The concept was launched by C.D. Keeling in the mid fifties, when he made several series of measurements in the USA. He found widely varying CO2 levels, sometimes in samples taken as short as 15 minutes from each other. He also noticed that values in widely different places, far away from each other, but taken in the afternoon, were much lower and much closer resembling each other. He thought that this was because in the afternoon, there was more turbulence and the production of CO2 by decaying vegetation and/or emissions was more readily mixed with the overlying air. Fortunately, from the first series on [ 2 ], he also measured 13C/12C ratios of the same samples, which did prove that the diurnal variation was from vegetation decay at night, while during the day photosynthesis at one side and turbulence at the other side increased the 13C/12C ratio back to maximum values.Keeling's first series of samples, taken at Big Sur State Park, showing the diurnal CO2 and d13C cycle was published in [ 7 ], original data (of other series too) can be found in [ 8 ]:As the oceans represent about 70% of the earth's surface, and all oceanic stations show near the same yearly averages and trends, already 70% of the atmosphere shows background behaviour (within 5 ppmv). This can be extended to near the total earth for the part above the inversion layer.Above land, diurnal variations are only seen up to 150 m (according to [ 7 ]).Seasonal changes reduce with altitude. This is based on years of flights (1963-1979) in Scandinavia [ 7 ] and between Scandinavia and California [ 9 ]. Further confirmed by old and modern [ 10 ] flights in the USA and Australia (Tasmania). In the SH, the seasonal variation is much smaller and there is a high-altitude to lower altitude gradient, where the high altitude is 1 ppmv richer in CO2 than the lower altitude. This may be caused by the supply of extra CO2 from the NH via the southern branch of the Hadley cell to the upper troposphere in the SH.From [ 7 ], based on [ 9 ]:As one can see, again the values above the inversion layer are near straight and agree within a few ppmv with the Mauna Loa data. Below the inversion layer, the morning values are 15-35 ppmv higher, in the afternoon, these may sink to background again.If we take the 1000 m as the average upper level for the influence of local disturbances, that represents about 10% of the atmospheric mass. Thus the "background" level can be found at 70% of the earth's air mass (oceans) + 90% of the remaining land surface (27%). That is in 97% of the global air mass. Only 3% of the global air mass contains not-well mixed amounts of CO2, which is only over land.General conclusion:(in high mountain ranges, this may be higher).This chapter is moved to its own page at co2_origin.html

[1] Carbon Dioxide Concentrations at Mauna Loa Observatory, Hawaii, 1958-1986, CDIAC NDP-001: http://cdiac.ornl.gov/ftp/ndp001/ndp001.pdf [2] Rewards and penalties of monitoring the earth, Charles D. Keeling, Ann. Rev. Energy. Envir. 1998.23.25-82: http://scrippsco2.ucsd.edu/publications/keeling_autobiography.pdf Fascinating autobiographic story from C.D.Keeling about the history of CO2 measurements and the struggle against the administrations to get and continue funding for continuous measurements.Of special interest:- First measurements on 5 l flasks were done with enhanced barometric equipment, with an accuracy of better than 0.1 ppmv.- The same barometric equipment was used to test calibration gases and NIR equipment. A change in calibration gases (air/CO2 vs. N2/CO2) caused a jump in response of the NIR equipment. All previous collected data were corrected for this change.