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The strong fluctuations in the net yearly anthropogenic CO fluxes into the atmosphere, are de- picted in Fig. 9. Figure 9: The correlation of yearly atmospheric CO2 changes (NOAA, 2022b) to the temperature changes of the southern oceans (NOAA, 2022c).

Figure 9 The strong fluctuations in the net yearly anthropogenic CO fluxes into the atmosphere, are de- picted in Fig. 9. Figure 9: The correlation of yearly atmospheric CO2 changes (NOAA, 2022b) to the temperature changes of the southern oceans (NOAA, 2022c).

Related Figures (11)

Figure 1: The carbon cycle presentation shows the recycling flux values of the IPCC (2021, Figure 5.12). The numerical values are reservoir amounts in gigatons of carbon (GtC); the flux values are in GtC yr!.
Figure 1: The carbon cycle presentation shows the recycling flux values of the IPCC (2021, Figure 5.12). The numerical values are reservoir amounts in gigatons of carbon (GtC); the flux values are in GtC yr!.
Figure 2: The observed permille value in the atmosphere versus the anthropogenic percentage according to the IPCC. The relationship is linear, and it has been continued to a theoretical situation that the atmospheric CO2zis totally anthropogenic.
Figure 2: The observed permille value in the atmosphere versus the anthropogenic percentage according to the IPCC. The relationship is linear, and it has been continued to a theoretical situation that the atmospheric CO2zis totally anthropogenic.
Table 1. The average CCFs (GtC yr') from 2010 to 2017, according to IPPC (2021, Fig. 5.12), and the percentage fraction of the anthropogenic COz from the total oceanic or terrestrial CCF. Table 1’s figures mean the ocean-atmosphere flux would not favour the atmosphere’s anthropo- genic fraction since it contains 32.0 % of this fraction, and in the atmosphere, its fraction is 32.1 %. Oppositely, the gross photosynthesis flux has only 20.4 % of anthropogenic CO2. Does a phys- ical explanation for these figures exist? The percentage of the ocean flux is close enough to the atmospheric composition but the percentage of the land plants figure is far too low. The plants prefer anthropogenic CO> for its higher '*C isotope concentration. Also, the ocean’s surface mix- ing layer favours anthropogenic CO: since phytoplankton and plants in the euphotic surface layer prefer the '°C isotope.
Table 1. The average CCFs (GtC yr') from 2010 to 2017, according to IPPC (2021, Fig. 5.12), and the percentage fraction of the anthropogenic COz from the total oceanic or terrestrial CCF. Table 1’s figures mean the ocean-atmosphere flux would not favour the atmosphere’s anthropo- genic fraction since it contains 32.0 % of this fraction, and in the atmosphere, its fraction is 32.1 %. Oppositely, the gross photosynthesis flux has only 20.4 % of anthropogenic CO2. Does a phys- ical explanation for these figures exist? The percentage of the ocean flux is close enough to the atmospheric composition but the percentage of the land plants figure is far too low. The plants prefer anthropogenic CO> for its higher '*C isotope concentration. Also, the ocean’s surface mix- ing layer favours anthropogenic CO: since phytoplankton and plants in the euphotic surface layer prefer the '°C isotope.
Figure 3: The observed decaying rate of '*C (blue curve) (LLNL, 2022), the simulation result of (Ollila, 2016) (red curve) for anthropogenic CO2, and the theoretical decaying rate of '4C without recycling fluxes in the carbon circulation system (black dashed curve). Radiocarbon isotope '“C from the nuclear bomb tests in the atmosphere accidentally created a global test for the carbon cycle system, and it can be considered the only full-scale climate test by humans, Fig. 3.
Figure 3: The observed decaying rate of '*C (blue curve) (LLNL, 2022), the simulation result of (Ollila, 2016) (red curve) for anthropogenic CO2, and the theoretical decaying rate of '4C without recycling fluxes in the carbon circulation system (black dashed curve). Radiocarbon isotope '“C from the nuclear bomb tests in the atmosphere accidentally created a global test for the carbon cycle system, and it can be considered the only full-scale climate test by humans, Fig. 3.
Figure 4: Permille trends from 1750 to 2020 for air to sea and sea to air. The observed atmospheric 6'3C (blue curve) and anthropogenic CO2 (green curve) trends in the surface ocean water (mixed layer) have been presented. These studies conclude that the exact knowledge of the numerical values of air-to-sea and sea-to- air fractionation numbers still varies among different research studies. However, general trends from 1750 to now, with accuracies of about + 0.5%o, can be estimated. The author has constructed simple equations for calculating yearly values for air-to-sea and sea-to-air fractionation trends. The curves based on these equations are explained in the attachment and the permille values ac- cording to these equations are depicted in Fig. 4.
Figure 4: Permille trends from 1750 to 2020 for air to sea and sea to air. The observed atmospheric 6'3C (blue curve) and anthropogenic CO2 (green curve) trends in the surface ocean water (mixed layer) have been presented. These studies conclude that the exact knowledge of the numerical values of air-to-sea and sea-to- air fractionation numbers still varies among different research studies. However, general trends from 1750 to now, with accuracies of about + 0.5%o, can be estimated. The author has constructed simple equations for calculating yearly values for air-to-sea and sea-to-air fractionation trends. The curves based on these equations are explained in the attachment and the permille values ac- cording to these equations are depicted in Fig. 4.
Figure 5: The simulation results by DAOBM-4 from 1750 to 2020.
Figure 5: The simulation results by DAOBM-4 from 1750 to 2020.
Figure 6: The carbon budget from 1750 to 2020. The carbon budget values starting from 1750 can be calculated using the DAOBM-4 model; essential values are collected in Fig. 6.
Figure 6: The carbon budget from 1750 to 2020. The carbon budget values starting from 1750 can be calculated using the DAOBM-4 model; essential values are collected in Fig. 6.
Figure 7: The observed 6!°C values of Mauna Loa are from CDIAC (2022b), and the reference 6'°C values are from Francey et al. (1999) and Rubino et al. 2013). The calculated 6'*C values and the anthropogenic CO? in the atmosphere are calculated by the model DAOBM-4. the total COz absorbed by the ocean, can be explained by the great amount of 180 GtC of natural CO2 moving into the atmosphere, and at the same time 252 GtC of anthropogenic CO2 absorbed by the sea. The atmospheric anthropogenic CO2 amount is only 70 GtC, which is 8 % of the total atmospheric CO2 mass originating from the direct fossil fuel emissions at 39 GtC, recycled from the biosphere at 27 GtC, and recycled from the ocean at 4 GtC in 2020. The basic reason for this is the continuous recycling of CO> fluxes between reservoirs, which removes and add anthropo- genic CO: into the atmosphere even without increasing sink values. The plants start releasing anthropogenic COz according to different delay times, as the Appendix equation (23) describes. Another important feature is that the major fraction of the increased atmospheric CO:2 increase is natural CO> originating from the oceans at 180 GtC and the biosphere at 35 GtC, totalling 215 GtC.
Figure 7: The observed 6!°C values of Mauna Loa are from CDIAC (2022b), and the reference 6'°C values are from Francey et al. (1999) and Rubino et al. 2013). The calculated 6'*C values and the anthropogenic CO? in the atmosphere are calculated by the model DAOBM-4. the total COz absorbed by the ocean, can be explained by the great amount of 180 GtC of natural CO2 moving into the atmosphere, and at the same time 252 GtC of anthropogenic CO2 absorbed by the sea. The atmospheric anthropogenic CO2 amount is only 70 GtC, which is 8 % of the total atmospheric CO2 mass originating from the direct fossil fuel emissions at 39 GtC, recycled from the biosphere at 27 GtC, and recycled from the ocean at 4 GtC in 2020. The basic reason for this is the continuous recycling of CO> fluxes between reservoirs, which removes and add anthropo- genic CO: into the atmosphere even without increasing sink values. The plants start releasing anthropogenic COz according to different delay times, as the Appendix equation (23) describes. Another important feature is that the major fraction of the increased atmospheric CO:2 increase is natural CO> originating from the oceans at 180 GtC and the biosphere at 35 GtC, totalling 215 GtC.
Figure 8: Decay rates of anthropogenic CO2 and total CO2 when fossil fuel emissions drop to zero after 2020. It can be estimated that after 1850, the model-calculated 8'°C values very accurately follow the atmospheric anthropogenic CO2 growth rate considering the opposite changes of these curves: These curves are like mirror images. Since the 5'°C value -28 %o of anthropogenic emissions dramatically differs from the ocean’s recycling flux, it dominates the atmosphere’s 5'°C value. Fig. 8 depicts the simulation results of DAOBM-4 for the anthropogenic CO and total CO2 in the atmosphere when the fossil fuel emissions drop to zero after 2020.
Figure 8: Decay rates of anthropogenic CO2 and total CO2 when fossil fuel emissions drop to zero after 2020. It can be estimated that after 1850, the model-calculated 8'°C values very accurately follow the atmospheric anthropogenic CO2 growth rate considering the opposite changes of these curves: These curves are like mirror images. Since the 5'°C value -28 %o of anthropogenic emissions dramatically differs from the ocean’s recycling flux, it dominates the atmosphere’s 5'°C value. Fig. 8 depicts the simulation results of DAOBM-4 for the anthropogenic CO and total CO2 in the atmosphere when the fossil fuel emissions drop to zero after 2020.
Therefore, FOtoranincreases from 75.0 GtCyr" in 1750 to 85.6 GtCyr' in 2020. Total dissolu- tion carbon pump flux FOjotup from the ocean into the atmosphere depends linearly on the sur- face ocean’s total CO concentration minus the same in 1750 per eq. (5). Therefore, FOtotup in- creased from 75.0 GtCyr' in 1750 to 83.5 GtCyr' in 2020. The linear dependencies of eq. (1) and eq. (5) means both fluxes increase as the total atmospheric CO: increases. Both fluxes di- minish into the 1750 value if the actual CO2 concentration values in the atmosphere or the sur- face ocean approach the values of 1750.
Therefore, FOtoranincreases from 75.0 GtCyr" in 1750 to 85.6 GtCyr' in 2020. Total dissolu- tion carbon pump flux FOjotup from the ocean into the atmosphere depends linearly on the sur- face ocean’s total CO concentration minus the same in 1750 per eq. (5). Therefore, FOtotup in- creased from 75.0 GtCyr' in 1750 to 83.5 GtCyr' in 2020. The linear dependencies of eq. (1) and eq. (5) means both fluxes increase as the total atmospheric CO: increases. Both fluxes di- minish into the 1750 value if the actual CO2 concentration values in the atmosphere or the sur- face ocean approach the values of 1750.
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