Research Article | Open Access
Radiation Transfer Calculations and Assessment of Global Warming by CO2
We present detailed line-by-line radiation transfer calculations, which were performed under different atmospheric conditions for the most important greenhouse gases water vapor, carbon dioxide, methane, and ozone. Particularly cloud effects, surface temperature variations, and humidity changes as well as molecular lineshape effects are investigated to examine their specific influence on some basic climatologic parameters like the radiative forcing, the long wave absorptivity, and back-radiation as a function of an increasing CO2 concentration in the atmosphere. These calculations are used to assess the CO2 global warming by means of an advanced two-layer climate model and to disclose some larger discrepancies in calculating the climate sensitivity. Including solar and cloud effects as well as all relevant feedback processes our simulations give an equilibrium climate sensitivity of = 0.7°C (temperature increase at doubled CO2) and a solar sensitivity of = 0.17°C (at 0.1% increase of the total solar irradiance). Then CO2 contributes 40% and the Sun 60% to global warming over the last century.
The Fifth Assessment Report (AR5)  of the Intergovernmental Panel on Climate Change (IPCC), a list of all abbreviations is found in the annex, announces new evidence of an anthropogenic climate change based on many independent scientific analyses from observations of the climate system, paleoclimate archives, theoretical studies of climate processes, and simulations using climate models. So, the IPCC classifies the human influence as extremely likely to be the dominant cause of the observed warming since the mid-20th century (AR5-WG1-SPM-D3). Increasing emissions of carbon dioxide (CO2) over the last century especially are made responsible for this change, and the equilibrium climate sensitivity (ECS or ) as a measure for the Earth’s temperature increase at doubled CO2 concentration in the atmosphere is specified to be likely in the range 1.5°C to 4.5°C (high confidence) (AR5-WG1-SPM, p16).
Although in all these fields of climate sciences great progress has been achieved over the last decades and our knowledge about the Earth-atmosphere system (EASy) could significantly be improved, explanations of the observed global warming over the last century in particular the anthropogenic contributions to this warming are still quite contradictorily discussed.
All the more it is surprising(i)that many of the consulted analyses and also the AR5 itself do not better and clearly distinguish between an anthropogenic emission of CO2 and a naturally generated part, where the latter even contributes more than 95% to the overall emission, and its generation rate and the respective absorption rate sensitively respond on global temperature variations;(ii)that the IPCC claims it would be extremely likely that more than half of the observed increase in global average surface temperature from 1951 to 2010 was caused by the anthropogenic increase in greenhouse gas concentrations and other anthropogenic forcings, while contributions from natural forcing and an internal variability both would only likely be in the range of −0.1°C to 0.1°C;(iii)that the meanwhile well known delayed response of CO2 and methane (CH4) to sea and air temperature changes (see, e.g., Petit et al. ; Monnin et al. ; Caillon et al. ; Torn and Harte ; Humlum et al. ; Salby ) are not considered in AR5, and respective consequences for an anthropogenic global warming are not discussed;(iv)that quite uncertain data about cloud feedbacks and studies of the radiative forcing (RF) of greenhouse (GH) gases are referred, which are mostly valid for clear sky conditions, while the introduction of clouds is usually omitted (AR5-WG1- Chap.8.3.1);(v)that the IPCC denies any noticeable solar influence on the actual climate, although strong evidence of an increasing solar activity over the last century exists (see, e.g., Hoyt & Schatten ; Willson & Mordvinov ; Shapiro et al. ; Ziskin & Shaviv ; Scafetta & Willson ; Usoskin et al. ; Zhao & Feng ; Soon et al. );(vi)that obviously important effects like convection and evaporation feedback, which can contribute to significant negative feedback (Harde-2014 ), are not considered in many analyses.Nevertheless, despite these deficits and simplifications the mean equilibrium climate sensitivity is specified with high confidence, and the GH gases are even assigned with very high confidence (95%) to be responsible for the actual climate changes.
Here we will focus on the assessment of one of the most important quantities in climate sciences and its validation, the ECS, which has to be scrutinized in more detail. Due to its far reaching consequences for future climate predictions it is particularly important to understand and to discover the large discrepancies between different accounting methods applied for this quantity. Also the weighting of some quite different and even counteracting processes which control our climate, but which are not always well understood, has carefully to be investigated with its implications on the climate sensitivity. A quite critical report of actually published ECS values and accounting methods expanded in AR5 has been published by Lewis and Crok .
In this contribution we will also retrace the main steps of the IPCC’s preferred accounting system and compare this with our own advanced two-layer climate model (2LCM), which is especially appropriate to calculate the influence of increasing CO2 concentrations on global warming as well as the impact of solar variations on the climate (Harde-2014 ). This model describes the atmosphere and the ground as two layers acting simultaneously as absorbers and Planck radiators, and it includes additional heat transfer between these layers due to convection and evaporation. It also considers short wave (sw) and long wave (lw) scattering processes at the atmosphere and at clouds; it includes all common feedback processes like water vapor, lapse rate, and albedo feedback but additionally takes into account temperature dependent sensible and latent heat fluxes as well as temperature induced and solar induced cloud cover feedback.
The objective of our studies is not to present a new only “true ECS” but to identify some of the different assumptions and approximations with their far reaching consequences in climate politics. It is without any doubt that the ECS is the most important measure for the CO2 influence on our climate, but it is also clear that this quantity does not distinguish between anthropogenic and natural CO2 emissions. Therefore, as long as any natural variations in the CO2 concentrations are not accurately known, the ECS cannot be used as a reliable indicator only for an anthropogenic global warming. All this in mind the reader may have his own reservations about the published data for this measure and its significance for a man-made climate change.
For the assessment of the ECS the IPCC favors the concept of radiative forcing (RF), which is supposed to be appropriate to describe the transition of the surface-troposphere system from one equilibrium state to another in response to an externally imposed perturbation. Therefore, in Section 2 we briefly outline some basic relations characterizing this concept, before we present in Section 3 detailed line-by-line radiation transfer (LBL-RT) calculations for the lw up- and downwelling fluxes in the atmosphere (for details see Harde [16, 18, 19]), this for clear sky, global mean cloud cover, full cloudiness, different surface temperatures, humidity, and even different lineshapes. These calculations were performed for the most important GH gases water vapor (WV), carbon dioxide, methane, and ozone and are based on the HITRAN08 database . Since the concentration of the GH gases and the atmospheric pressure are changing with temperature and altitude, the atmosphere has to be segmented into up to 228 sublayers from ground to 86 km height and in some cases additionally into three climate zones. When these computations are repeated for different CO2 concentrations at otherwise same conditions, from the changing fluxes on the one hand the CO2 initiated RF as the main parameter for the IPCC accounting scheme and on the other hand the sw and lw absorptivities as well as the back-radiated fraction of the atmospheric emission as the key parameters in our 2LCM can be derived.
Section 4 summarizes the main features of the 2LCM and its calibration to satellite data, for the radiation and heat fluxes using the well known radiation and energy budget scheme of Trenberth et al. , for temperature changes due to cloud cover variations applying the observations within the International Satellite Cloud Climatology Project (ISCCP) . With the respective key parameters of Section 3 integrated in the climate model we simulate the Earth’s surface temperature and the lower tropospheric temperature as a function of the CO2 concentration. The temperature increase at doubled CO2 concentration then directly gives the CO2 climate sensitivity. Such simulations reproduce the direct or basic ECS value (without feedback processes), as specified by the IPCC, within better than 10%. Significant differences, however, can be observed with the different feedback effects included. Our investigations show the largest discrepancies for the WV and cloud feedback, but they also disclose the importance of one of the primary stabilizers of the whole climate system, the evaporation feedback. Therefore, these processes and their contributions are extensively analyzed under different humidity, surface temperature, lapse rate, and cloud cover conditions.
In particular, these studies show that the observed cloud changes within the ISCCP cannot exclusively be explained by pure thermally induced cloud cover changes but obviously are additionally controlled by a further cloud forcing mechanism. Since there exists strong evidence that the solar activity also has a powerful influence on the cloud cover, it is reasonable to postulate such a solar induced cloud feedback (see, e.g., Svensmark ; Haigh ). This is investigated in detail in Section 5, differentiating between a pure thermal impact of an increasing solar activity and a nonthermally induced solar cloud feedback. An important criterion for a validation, which mechanism might control such cloud changes, can be derived from model simulations, which include the solar anomaly over the last century and compare this directly with the observed global warming over this period. These investigations indicate that due to the strong cloud feedback the observed warming over the last century can only satisfactorily be explained, attributing a significant fraction to the increased solar activity over this period (see also Ziskin & Shaviv ; Vahrenholt & Lüning ).
Our simulations predict a solar contribution of about 60% and a CO2 induced contribution of 40% to global warming over the last century with an equilibrium climate sensitivity of 0.7°C, which is almost a factor of five smaller than published in AR5.
2. Radiative Forcing
The concept of RF is well established in climate sciences and used to assess the global warming as a result of an external perturbation of EASy (AR5-WG1-Chap.8). This perturbation can result from solar anomalies, from increased GH gas concentrations or volcanic activities. In all cases a direct proportionality of the Earth’s temperature increase Δ as response to an external forcing is assumed in the form with as the climate sensitivity parameter, also known as Planck sensitivity. The negative reciprocal of is called the Planck feedback (see AR5-WG1-Chap.9), although this is not a feedback process in the common sense like the water vapor, the albedo, or lapse rate feedback, which all describe an internal amplification or attenuation of an external perturbation. The Planck feedback rather represents the change of the outgoing long wave radiation (OLR), or more precisely the change of the total upwelling lw intensity with the ground temperature. Since an increasing amount of OLR with the temperature causes a negative feedback for EASy, it can be defined as the negative partial derivative as follows:Its value, deduced as an average from different climate models, is given in AR5-WG1-Tab.9.5 as −3.2 W/m2/°C, and, thus, the Planck sensitivity becomes = 0.31 W−1 m2°C. A somewhat simplified method to assess the Planck feedback and sensitivity, which agrees within 15% with these values, is to use the slope of the Stefan-Boltzmann law at an effective Earth temperature = 255 K and emissivity withand to assume the same temperature response for the surface as for the atmosphere. This results in a Planck feedback of −3.76 W/m2/°C and a climate sensitivity parameter = 0.27 W −1 m2°C. is the Stefan-Boltzmann constant with 5.67·10−8 W/m2/°C4 and the OLR with 239.4 W/m2.
Eq. (1) is the basis for many climate models (see AR4  and AR5 ) and even for more complex models like the Atmosphere-Ocean-General-Circulation Models (AOGCMs) this fundamental relation is used to express the influence of the growing GH gas concentrations on the surface temperature. So, for these models and also for the observationally based energy budget ECS estimates (see, e.g., Forster & Gregory ; Lindzen & Choi ) is a quite fundamental quantity, which cannot directly be measured but has to be deduced from extensive spectroscopic calculations or solar data, which on their part rely on many individual observations and measurements. For quite actual investigations of see also Feldman et al. .
In this context it should be noticed that alternative definitions of RF have been developed, each with its own advantages and limitations (see AR5-WG1-Chap.8). Here we only consider the instantaneous RF, which refers to an instantaneous change in the net (down minus up) radiative flux (sw plus lw) due to an imposed change. This forcing is usually defined in terms of flux changes at the top of the atmosphere (TOA) or at the tropopause.
In this contribution, particularly the influence of CO2 on global warming is of interest. Therefore, in the next subsection we present some actual radiation transfer (RT) calculations, from which the instantaneous RF due to increasing CO2 in the atmosphere and also some related quantities, which are of relevance for our two-layer climate model, can be derived. Since for these model calculations it is not sufficient only to consider the net radiative fluxes at the tropopause, neglecting the downwelling absorption changes in the troposphere and the upwelling absorption changes over the stratosphere, we apply the RT concept from the surface to TOA and vice versa. The sw absorption changes over the full atmosphere and this as a function of the CO2 concentration can be captured from our previous investigations (Harde-2014 ).
As already outlined, an important reference for the influence of CO2 is the temperature increase at doubled CO2 concentration under steady state conditions, which is known as the equilibrium climate sensitivity ECS or , and the respective lw forcing may be designated as . Since at TOA a lw downwelling flux is zero, the forcing at TOA can be defined as difference of the total outgoing intensities at single and doubled CO2 concentration :where here we primarily consider the lw radiative forcing. can be explained to consist of the nonabsorbed terrestrial intensity () plus the emitted intensity of the atmosphere in upward direction ; thus, it holds the following:with is the intensity of the incident terrestrial radiation and the absorbed flux in the atmosphere.
So, due to (4) this forcing generally consists of two contributions, the change in the upward atmospheric emission and the change in the atmospheric absorption of terrestrial radiation, both as response to a doubling of the CO2 concentration.
Expressing the downwelling atmospheric intensity via the total emitted intensity and the fraction , which is directed downward (also called asymmetry factor of the emitted atmospheric radiation) and which is generally found from integrating the respective spectral intensities at TOA and the surface over the frequency or reciprocal wavelength (wavenumber) withthe difference between single and doubled concentration giveswith and as the respective differences of and at single and doubled CO2 concentration.
Then, with (7), for the difference of the upwelling atmospheric intensities we can write and the radiative forcing at doubled CO2 concentration can finally be expressed as follows:This CO2 forcing can directly be derived from radiation transfer calculations (Schwarzschild [30, 31]; Goody and Yung ; Salby-2012 ; Harde-2013 ; Harde-2014 ), by which the up- and downwelling fluxes as well as the absorption and emission in the atmosphere are computed.
3. Radiation Transfer Calculations
Since it is obvious that the cloud cover has a strong influence on the up- and downwelling fluxes in the atmosphere and also on the strength of the GH effect, we have performed line-by-line radiation transfer (LBL-RT) calculations under different cloudiness conditions, ground temperatures, and humidity to evaluate the influence of CO2 on global warming. We also briefly investigate the influence of lineshape effects on RT calculations and their consequences for the ECS.
Here we only present global RT calculation with averaged values for the temperature, water vapor concentration, and an average lapse rate, since separate computations for the tropics mid- and high-latitudes with individual profiles and averaging over the climate zones with an area weighting factor gave almost the same results (see also Harde ).
3.1. Clear Sky at Global Mean Temperature
Table 1 shows the results of our LBL calculations under clear sky conditions as a function of the CO2 concentration, using a ground temperature of = 289.15 K = 16°C and a terrestrial intensity of = 396 W/m2. These values are consistent with those used by Trenberth et al. .
As an average over the three climate zones the water vapor concentration at ground was assumed to be 14,615.3 ppm and decreasing with altitude due to the Clausius-Clapeyron equation (for details see Harde-2014 ). These data have been derived from satellite measurements (Vey ) and are almost a factor of two larger than those given by the US Standard Atmosphere . But they are in quite good agreement with the Average Global Atmosphere (Ollila ), which even specifies values 12% larger than ours. The CH4 concentration was set to 1.8 ppm and to vary over the stratosphere with a maximum concentration of 7 ppm at 38 km altitude. The lapse rate and pressure variation with altitude agree with the US Standard Atmosphere.
Our calculations cover a spectral interval from 10 to 2500 cm−1, corresponding to 99.86% of a Planck radiator at , and they include more than 78,000 lines with spectral intensities larger 10−24 cm−1/(molecules·cm−2). The spectral resolution for calculations at CO2 concentrations of 380 and 760 ppm, which are used as reference data, was chosen as 0.07 cm−1 (2.2 GHz), and for the vertical direction 228 sublayers were distinguished, whereas the calculations at the other concentrations were performed with half the spectral and vertical resolution.
Comparison of the two last values in column 2 of Table 1 shows that within rounding errors (9) is well confirmed. Looking at the upwelling intensity of the atmosphere (column 3) we see that this is almost identical at single and doubled CO2 concentration, while the downwelling part (column 4) and the total atmospheric radiation (column 5) both are increasing by more than 4.4 W/m2. This means that at clear sky conditions most of the additionally absorbed terrestrial radiation at doubled CO2 (see column 6) is instantaneously directed back to the surface, and only a relatively small contribution of 0.6 W/m2 is trapped in the atmosphere.
Since in this case the first two terms in (9) almost exactly compensate each other, the forcing under clear sky conditions is in good approximation only determined by the absorption difference. Thus, from the simple radiative forcing model (1) it follows that also the ground temperature variations are almost only determined by this additionally absorbed power.
In general, however, it should be clear that the surface temperature also depends on the emission characteristic of the atmosphere, which changes with the GH gas concentration as well as with the cloud cover and is determined by the first two terms in (9). Only under clear sky they just feed most of the additionally absorbed power back to the surface.
In a more advanced model, as this will be discussed later with a radiation and energy balance at TOA and at the surface, including heat fluxes of sensible and latent heat or from neighbouring climate zones, as well as sw and lw absorption losses, even at clear sky conditions the atmospheric emission characteristic is of relevance, which can well be represented by the fraction of the downward emitted radiation.
The relative absorption of terrestrial radiation by the GH gases and its variation with increasing CO2 concentration are listed in column 7. It is normalized to the incident terrestrial flux and in this way represents the lw absorptivity as defined in Harde-2014  (). This absorptivity is represented in Figure 1 (black diamonds) together with the back-radiated fraction of the atmosphere (blue triangles). At higher concentrations both quantities can well be represented by logarithmic graphs (magenta line for , green line for ), indicating that due to saturation effects then only the far wings will further contribute to an increasing absorption or emission.
3.2. RT Calculations at Clear Sky and Increased Surface Temperature
Whereas the above calculations reflect a somewhat artificial situation, assuming clear sky and a global mean temperature of 16°C, we know that with declining cloud cover the average surface temperature is significantly climbing up. So, from observations within the International Satellite Cloud Climatology Project (ISCCP)  it is found that around the global mean cloud cover of 66% a reducing cloudiness of 1% causes a temperature increase of about 0.06–0.07°C, a tendency which is also confirmed by data of Hartmann .
Therefore, to get a better understanding of how such higher temperature modifies the respective fluxes in the atmosphere and especially this affects the CO2 radiative forcing, we have performed additional calculations for a surface temperature of 20.3°C. At this temperature and a surface emissivity of 100% the terrestrial radiation climbs up to 420 W/m2. But with the higher temperature also the humidity increases and therefore affects the absorptivity of the GH gases. From the measured water vapor concentrations as well as the temperatures at mid-latitudes and the tropics we deduce at the higher temperature a growth of the vapor concentration of 3,738 ppm with a new total mean concentration near the surface of 18,353 ppm.
Calculations for this higher ground temperature and water vapor concentration are shown in Table 2.
Since for an evaluation of CO2 with its influence on the radiation budget it is sufficient to concentrate on the fluxes at single and doubled CO2 concentration, here we only present this reduced data set. Compared to the lower temperature calculations the radiative forcing increases by 0.4 W/m2, which is mainly due to changes in the upward atmospheric emission with = 0.7 W/m2, while the absorption changes with = −4.8 W/m2 are even getting slightly smaller. Also the downward directed flux change with = −4.3 W/m2 and the total atmospheric emission change with = −3.6 W/m2 are reducing, although the absolute fluxes and the absorption are considerably larger, caused by the higher temperature and water vapor.
The absorptivity as calculated under these modified conditions is shown in Figure 2 (black diamonds) together with the back-radiated fraction of the atmosphere (blue triangles). At higher CO2 concentrations both graphs can again well be approximated by logarithmic functions, similar to Figure 1 (magenta line for , green line for ), only on slightly shifted scales.
3.3. LBL-RT Calculations at Global Mean Cloud Cover
Under regular cloud cover significant changes from clear sky conditions have to be expected for the up- and downwelling fluxes due to the strong shielding effect of clouds not only for sw but also for lw radiation. In our radiation transfer calculations the clouds are considered as a single thinner layer, which absorbs the incident lw radiation from up or down direction with a cloud absorptivity and which has a transmissivity of , while lw scattering processes at the clouds are here neglected. For the RT calculation only the resulting attenuation of radiation, which passes the layer, is of relevance, and for these calculations it is sufficient to express the total attenuation uniformly only by one parameter, the cloud absorptivity. In addition to the transmitted radiation the clouds are also emitting as a Planckian radiator with an emissivity and a temperature determined by the cloud altitude.
The Global Energy and Water Cycle Experiment (GEWEX) Radiation Panel, which compares the available global long-term cloud data products with the ISCCP and consists of 12 satellite measurement teams, specifies the global total cloud amount between 56% and 74% (Stubenrauch et al. ), where this relatively wide range is mainly explained by different instrument sensitivity and by retrieval methodology. For our further calculations we assume a global mean cloud cover of = 66% in agreement with the ISCCP . The cloud altitude with = 5.1 km and the emissivity with = 63% were chosen to almost exactly reproduce the widely accepted radiation and energy budget scheme of Trenberth et al.  (hereafter called TFK-scheme) with a total upward flux of and a nonabsorbed outgoing radiation from the surface with .
Our RT calculations under otherwise identical conditions as described in Section 3.1 and at a surface temperature = 16°C are listed in Table 3. They show significant changes to the radiation fluxes under clear sky, for example, for , more than 20 W/m2 or for even 28 W/m2. Also the total absorption, now additionally increased by the clouds, is 31 W/m2 larger than at clear sky.
But respective differences between single and doubled CO2 concentrations, which are here of main interest, in general are getting smaller. So, the radiative forcing reduces to = 3.77 W/m2 and is almost identical with the figure used by the IPCC (Myhre et al. ), although here we consider only the instantaneous lw RF at TOA. This forcing is the result of the upwelling atmospheric contribution of and on the other hand a reduced absorption difference of compared to −5 W/m2 at clear sky. Also changes in the back-radiation diminish from −4.5 W/m2 to and the total emission even from −4.4 W/m2 to .
Because of this smaller alteration in the atmospheric emission the 1st term in (9) with now reduces to −0.99 W/m2, whereas the 2nd term with = 1.83 W/m2 dominates. From the total forcing of 3.77 W/m2 in this case 3.45 W/m2 goes back to the surface, while 0.32 W/m2 remains in the atmosphere.
To deduce the lw absorptivity at cloudiness from the radiation transfer calculations, the absorbed intensity listed in column 6 of Table 3, which now reflects the total absorption caused by the GH gases and the clouds, has to be reduced by the cloud fraction. Such correction seems appropriate for a direct comparison of the absorptivity changes caused by the GH gases at clear sky and clouds, and it is necessary for our two-layer climate model, where the cloud absorption is already integrated in the model and represented by respective parameters. Such a correction is done by comparing the absorption, for example, at 380 ppm with and without clouds at the same ground temperature, and reducing column 6 by this difference. Normalizing the corrected absorption to the incident radiation then gives in good approximation the lw absorptivity of the GH gases in the presence of clouds.
Figure 3 shows the respective absorptivity (black diamonds) and the back-radiated fraction (blue triangles) at a cloud cover of 66%. Again both quantities can well be represented by logarithmic graphs (magenta line for , green line for ). While slightly increases by 0.8%, Δ remains constant. However, the absorptivity changes almost decline by a factor of two to −0.74% at doubled CO2 concentration.
Simulations at higher cloud altitudes under otherwise same constrains give a reduced upwelling flux and a further diminishing radiative forcing .
3.4. RT Calculations with MRT Lineshape
While the preceding calculations are based on the standard molecular collision theory, considering collisional broadening of spectral transitions, which are characterized by a Lorentzian lineshape or at higher altitudes also by a Voigt profile, we have also performed extensive calculations using a more sophisticated lineshape as given by the molecular response theory (MRT) (Harde et al. [40–44]). This theory represents a generalization and unification of the classical collision theories of Lorentz and on the other hand of van Vleck and Weisskopf, considering thermalization of molecules during a collision, which in its limit is determined by the reciprocal of the molecular transition frequency and controlled by Heisenberg’s uncertainty principle (Harde & Grischkowsky ). The specialty applying MRT is that it not only describes the near resonance absorption and emission behavior as already adequately characterized by a Lorentzian, but also reflects the far wing response, which is mainly caused by the ultrafast time response of molecules to an external electric field during collisions. So, the MRT lineshapes already represent very well the continuum water vapor absorption extending up to 1200 cm−1 and caused by the low frequency water vapor absorption band around 200 cm−1 (see Burch & Gryvnak ; Roberts et al. ).
This continuum water vapor background together with the far wing contributions of the other molecules significantly modifies the absolute up- and downwelling fluxes. Therefore, to further satisfy the radiation and energy balance of the TFK-scheme, in the radiation transfer calculations the cloud altitude has to be increased to 6 km and the cloud absorptivity = emissivity reduced to 47.8%.
The results of such a calculation at a mean cloud cover of 66% and at otherwise same conditions as described in Section 3.3 is shown in Table 4. To compare the alterations caused by doubling the CO2 concentration it is again sufficient only to display the calculations for 380 and 760 ppm CO2. It is interesting to see that the more sophisticated lineshape and the continuum background absorption almost have no influence on , the RF at doubled CO2, which agrees within better than 1% with the simpler calculations shown in Table 3, neglecting the continuum absorption and using a Lorentzian lineshape. Also changes in the other fluxes at doubled CO2 concentration are consistent within 0.1 W/m2; only the back-radiation changes to and is about 0.3 W/m2 smaller; thus, the power left in the atmosphere increases by this amount.
For this insensitivity to a different collision and lineshape theory we see three main reasons: first, because of the larger absolute flux variations, caused by the different wing absorption and WV continuum, the outgoing fluxes were recalibrated to the TFK-scheme via cloud altitude and absorptivity to ensure comparable absolute fluxes in agreement with the observations. Second, we only consider flux differences at single and doubled CO2 concentration for the same shape, so that discrepancies to another shape are not directly observed and smaller absolute variations with the CO2 concentration are to some extent cancel out. Third, the interference of the CO2 spectrum with strong water vapor lines and the underlying WV continuum further attenuates any CO2 lineshape effects.
So, calculations based on the classical collision theory obviously reproduce quite reliable data of any radiation changes in the atmosphere. Since the far wings of the CO2 lines are found to decay more rapidly than a Lorentzian and thus should contribute less to the total absorption (see, e.g., Edwards and Strow ), such calculations even simulate slightly worse conditions and result in a more conservative assessment of global warming by CO2. For actual CO2 lineshape studies see also Happer , and for RT calculations including CO2 line mixing see Mlynczak et al. , and Ozak et al. .
3.5. RT Calculations for Total Cloud Cover
With a further increasing cloud cover and thus a stronger shielding of the sw radiation also the surface temperature further drops, and owing to the ISCCP observations at 100% cloudiness then a reduced temperature of approximately 2.2°C compared to mean cloudiness is expected.
Respective radiation transfer calculations at 100% cloud cover, a surface temperature of 13.8°C with a terrestrial intensity of 384 W/m2, and a further reduced water vapor concentration at ground of 12,703 ppm, otherwise using the same conditions as in Section 3.3, are shown in Table 5. The total outgoing radiation drops by 15.4 W/m2 and the total atmospheric emission by 6.6 W/m2 compared to a cloud cover of 66%. Nevertheless, the forcing due to doubled CO2 reduces to = 3.0 W/m2, consisting of a slightly increasing contribution and a decreasing absorption . Also the absolute downwelling radiation further decreases by 5.2 W/m2, and its alteration at doubled CO2 concentration reduces to −2.9 W/m2, so almost nothing remains in the atmosphere.
The absorptivity as listed in column 7 is again found by comparing the absorption at 380 ppm with clouds (357.86 W/m2) and without clouds (313.57 W/m2), reducing column 6 by this difference and then normalizing the corrected absorption to the incident radiation. is shown together with the parameter in Figure 4. Both graphs can again well be represented by logarithmic plots.
The changes in absorptivity from single to doubled CO2 with = −0.5% further decline compared to 66% cloudiness or clear sky, and also is slightly reducing to −0.34%.
So, from these calculations it is clear that the up- and downwelling fluxes and also the absorption in the atmosphere are significantly varying with the cloud clover and, therefore, they will also significantly influence the global mean surface temperature. But it can also well be recognized, that changes with the CO2 concentration by trend get smaller with increasing cloudiness.
4. Assessment of CO2 Global Warming
Different to general circulation models, which try to predict local climate variations over some time period and, therefore, have to solve complex coupled nonlinear differential equations with a large number of parameters, making these calculations extremely time consuming and even unstable, for computing the equilibrium climate sensitivity it is sufficient to rely on a much simpler model, which calculates an equilibrium energy and radiation balance and averages over larger local variations.
But independent of the model’s complexity, almost all known models are based on the simple relation given by (1) that the ground temperature is scaling proportional with the radiative forcing of an external perturbation. Any feedback processes, for example, by water vapor, albedo, the lapse rate, or clouds, are generally included in this equation as an additional prefactor ()−1 in the following form:where is the feedback parameter, by which all linear and nonlinear responses of EASy to a changing surface temperature are represented (see also Lindzen & Choi , only using different symbols).
Thus, the simplest way to assess is to directly apply (10) with the known feedback and radiative forcing. Often, however, this calculus method suffers from the fact(i)that the Planck sensitivity has to be adapted from other models;(ii)that it is difficult to distinguish between different forcings with different feedbacks;(iii)that this method only considers a radiation balance at the tropopause or TOA, but not an additional radiation and energy balance at the surface;(iv)that it does not consider the feedback of the atmosphere to the surface and vice versa, caused by radiation changes as well as changes of sensible and latent heat;(v)that some feedback processes and their evaluation are not really retraceable from other sources;(vi)and that for simplicity reasons often sw feedback effects are completely neglected.Therefore, here we use our own advanced two-layer climate model, which is free from these deficits and which then can be compared with the IPCC accounting scheme or other methods. In addition, we investigate the effect and the size of the slightly changing reradiation of the atmosphere with increasing CO2 concentration as represented by the back-radiated fraction .
4.1. Model Adaptation to Satellite Measurements
Our two-layer climate model is especially appropriate to calculate the influence of the increasing CO2 concentrations on global warming as well as the impact of solar variations on the climate. The model describes the atmosphere and the ground as two layers acting simultaneously as absorbers and Planck radiators. It includes additional heat transfer between these layers due to convection and evaporation, and it considers cloud effects for the sw and lw radiation as well as all relevant feedback effects like water vapor, lapse rate, albedo, cloud cover, convection, and evaporation. At equilibrium both the atmosphere and the ground release as much power as they absorb from the Sun and the neighbouring layer. An external perturbation, caused by variations of the solar activity or the GH gases, then forces the system to come to a new equilibrium with new temperature distributions of EASy. Figure 5 shows the main features of the two-layer climate model with its relevant parameters.
Different to other schemes, in our model the key parameters are not the radiative forcing, but the sw and lw absorptivities and as well as the back-radiated fraction of the atmosphere , all of which are varying with the CO2 concentration (see Figures 1–4). Whereas the sw absorptivity can well be adopted from our previous calculations (Harde-2014 ), for the actual simulations we use the new and more advanced radiation transfer calculations, presented in Section 3, which clearly distinguish between clear sky and cloudy conditions. All other parameters like the cloud and sw ozone absorptivities, the scattering coefficients at clouds and the atmosphere, and the Earth’s reflectivities were adapted in such a way that all radiation and heat fluxes almost exactly reproduce the widely accepted TFK-scheme (see also Harde-2014 , Fig. 10), which essentially relies on data from satellite measurements within the ERBE and CERES program [51–55]. This adaptation yields a calibration of our model to the observed up- and downwelling fluxes under standard conditions in the atmosphere and for constant heat fluxes between the surface and atmosphere. All relevant parameters are listed in Table 6.
Compared to our previous simulations (Harde-2014 ) some of these parameters had slightly to be modified to further reproduce the TFK-scheme, this as a consequence of the changing fluxes and absorptivities with the ground temperature at clear sky or cloudiness. Particularly to reproduce the measured temperature variations with the cloud cover, the parameters and had to be adjusted to satisfy the TFK, as well as the ISCCP observations. In this sense our model is similar to the energy budget ESC estimates, which provide an independent observationally based constraint of this important parameter (see Lewis & Crok , Forster & Gregory , and Lindzen & Choi ).
For the temperature response of EASy and, thus, the calibration of the model we relate to the temperature anomaly data of the Hadley Centre and Climate Research Unit (HadCRUT3) as a function of the monthly global cloud cover data of the ISCCP (scatter diagram of O. Humlum, http://www.climate4you.com/ ) with a response of −0.065°C/%, while a reverse scatter plot for the same ISCCP data over the Berkley Earth Surface Temperature (BEST) leads to a much stronger temperature variation with cloud cover of about −0.3°C/%. Consequences for a thermally induced cloud cover feedback will be discussed in Section 4.3.6.
Our climate model also contains a parameter for the lw scattering at clouds () with the ability of multiple reflections between clouds and the surface. Since this quantity has no meaning in an RT calculation, considering only a one way propagation of radiation, the respective adaptation of the total upward flux and direct flux from the surface had to be fitted in the RT calculations via the cloud absorptivity , which, therefore, differs from the absorptivity used in the 2LCM.
The up- and downward fluxes as calculated by the two-layer climate model are compiled in Table 7 and show the excellent agreement with the TFK data. The smaller deviations mainly result from the fact that the fluxes in the TFK-scheme are not completely balancing in up- and downward direction but contribute to a net surface absorption of 0.9 W/m2, while our calculations are valid for steady state conditions with an exact balance between the absorbed solar radiation and the OLR.
It should also be noticed that the direct flux from the surface to TOA with 40 W/m2 can only be realized with a relatively high lw cloud scattering and medium cloud absorption. These parameters mainly determine the reference temperature and lw fluxes but have negligible influence on calculations of the ECS. So, for example, for = 0 and = 77%, for which the direct flux declines by 6 W/m2, while the indirect flux increases by the same amount, the climate sensitivity stays the same.
Since the objective of our investigations here is to evaluate the influence of CO2 on global warming, the parameters in Table 6 and the fluxes in Table 7 primarily define a working point for further considerations; in particular they determine the reference temperature = 16°C of the Earth’s surface at a CO2 concentration of 380 ppm. Only deviations from this reference, caused by a changing CO2 concentration and the different feedback processes, are of further interest, not so much absolute temperature levels.
4.2. Direct Influence of CO2
First we consider the simplest case, neglecting any feedback processes and looking only to the direct influence of CO2 on global warming. With the sw and lw absorptivities as well as the back-radiated fraction integrated in the climate model, the Earth’s surface temperature and the lower tropospheric temperature are simulated as a function of the CO2 concentration. For details, how these temperatures are calculated by the 2LCM and how they are defined, see Harde-2014 , Subsection .
For the case of clear sky ( = 0) this is shown in Figure 6(a), where the red graph indicates Earth’s temperature at the surface and the blue graph the lower tropospheric temperature as derived from the Stefan-Boltzmann relation when inserting the back-radiated power. The increase of at doubled CO2 concentration (from 380 to 760 ppm) defines the CO2 climate sensitivity as a measure for the response of EASy on a changing CO2 concentration. At clear sky conditions and without feedback effects this climate sensitivity is found as = 1.79°C, which is significantly larger than our previously published value of 1.1°C (Harde-2014 ).
The reason for this discrepancy is twofold. So, the new RT calculations (see Section 3.2) were performed for a ground temperature at clear sky of 20.3°C, which increases the lw absorptivity due to water vapor and, thus, lifts the climate sensitivity by about 0.4°C. Another contribution of 0.3°C is initiated by the back-radiation, which slightly changes via with the CO2 concentration (Figure 2). Although at clear sky the radiative forcing is almost only determined by the absorption losses in the atmosphere (see Table 2), the small variation Δ of less than 0.4%, multiplied with the total atmospheric emission , causes this additional increase in our model (see second term in (9)).
A higher cloudiness not only reduces the average surface temperature but also diminishes the climate sensitivity. This can be seen from Figures 6(b) and 6(c), showing the surface and atmospheric temperature at the mean cloud cover of 66% and 100% as a function of the CO2 concentration. At 66% cloudiness the climate sensitivity declines to = 1.09°C, while at 100% it even reduces to 0.89°C.
The green graphs in Figure 6 represent logarithmic fits, indicating that due to saturation effects and only far wing absorption at higher CO2 concentrations the surface temperature can well be approximated by a logarithmic function of the following form: where is the temperature at a CO2 concentration = 380 ppm, is the Planck sensitivity as it results from our two-layer climate model, and α is defined as (see also Myhre et al. ).
For the special case , (11) merges into (1), and we see that either can be derived from a logarithmic fit to the temperature data or from the climate sensitivity using (1). Table 8 summarizes the related quantities, which characterize the influence of CO2 on global warming under different cloud situations, but neglecting feedback processes. From these data we can assert that the Planck sensitivity, as deduced from our two-layer model, agrees within 8% with the model mean of the Coupled Model Intercomparison Project Phase 5 (CMIP5) AOGCMs (AR5-WG1-Tab.9.5) and is slightly varying with the cloud cover. The same holds for the reciprocal value, the Planck feedback.
In this context it should be emphasized that the climate sensitivities from our model were derived with the sw absorptivity changes included, while in (11) only represents the lw RF at TOA, different to AR5.
While the declining temperatures are a direct consequence of the dominating shielding effect for solar radiation, the smaller sensitivities are the result of the increasing influence of the lw cloud absorption and backscattering, by which the importance of the GH-gases is more and more repelled.
We also see that in comparison to the surface the lower atmosphere is responding less sensitively to the CO2 changes. This may be explained due to the changing radiation and energy balance between the surface and atmosphere with an increasing up- and downward emission of the atmosphere. But the difference between the two curves is more and more reducing at higher cloudiness.
4.3. Feedback Processes
Many climate models agree within acceptable limits in their prediction for the CO2 climate sensitivity, as long as feedback effects are excluded. But big discrepancies can be observed, when different feedback processes and also climate drivers are included. One reason may be the complexity of these effects, from which their interrelated actions and their mutual interference are not really known. Another reason can also be a wrong or undifferentiated assignment of the feedbacks to a specific climate driver, or the simple neglect of an effect.
In this subsection we first consider the influence and size of the well known feedback processes caused by water vapor, the lapse rate, or albedo. Further we investigate the additional effects of convection, evaporation, and cloud cover feedback, which in this form are not discussed and the first ones are even not mentioned in AR5.
4.3.1. Water Vapor Feedback
Water vapor (WV) is by far the largest contributor to the natural GH effect and, therefore, plays an essential role in Earth’s climate (AR5-WG1-Chap.8.1). Since its amount in the atmosphere is only controlled by the air temperature, rather than by emissions, scientists consider it as a feedback agent, rather than a forcing to climate change.
In AR5 we read as follows: “the contribution of water vapor to the natural greenhouse effect relative to that of CO2 depends on the accounting method, but can be considered to be approximately two to three times greater.” With respect to their relative concentrations in the atmosphere this proportion appears very small, as an amplifier for the basic climate sensitivity; however, it is quite significant and has to be investigated in more detail.
Indeed, different methods can be applied to estimate this ratio, and their results deviate significantly, depending on what is made responsible for the GH effect and its definition. So, similar to the procedure used to determine the RF at doubled CO2, one way is first to calculate the total upwelling intensity without WV, , minus the intensity with all GH gases in the atmosphere . At global mean cloud cover and with MRT lineshapes (see also Table 4) this gives a difference . Next one has to calculate the difference between the intensities without CO2 and with all gases yielding . Comparison of these differences gives a ratio of 59/23.6 = 2.5 in good agreement with AR5. However, this method essentially characterizes the efficiencies of these gases to block the OLR to space, and thus primarily reflects the radiation balance at TOA, but not so much at the surface.
Therefore, another way of accounting is to consider the differences of the downwelling intensities, which at cloudiness result in and with a ratio 190.1/14.4 = 13.2. This method is particularly sensitive to the contributions of WV or CO2 at the surface and shows the dominating influence of WV in the lower troposphere, which in this accounting scheme contributes about 60% to the GH effect, while CO2 is donating not more than 4% and thus relativizes the importance of CO2 as a dangerous climate driver in the atmosphere. An even slightly larger ratio of WV to CO2 to the GH effect of about 14 can be found, when calculating the back-radiation under clear sky conditions. A similar result is found considering only the absorption of the terrestrial radiation, first for all gases and then without one of the components, yielding a weighting ratio of 15.
With respect to feedback processes these numbers look quite dramatic. But the contribution of a gas or vapor to the GH effect does not automatically determine its influence as a feedback agent. Therefore, this has to be considered more extensively.
Due to the Clausius-Clapeyron equation the WV content is rapidly increasing with rising temperatures. So, from GPS-measurements (Vey ) of the water content in different climate zones we can derive the average WV concentration in a zone (see Harde-2014 , Fig. 1), and with the temperature differences between these zones we then estimate that with every extra degree of air temperature the atmosphere retains 5.9% more water vapor. Therefore, also the WV absorption is further increasing and generally contributes to a positive feedback in the total budget. In the literature this feedback is designated as the most serious effect with dramatic amplification values. So in AR5-WG1-Chap.8 we can read “although CO2 is the main anthropogenic control knob on climate, water vapor is a strong and fast feedback that amplifies any initial forcing by a typical factor between two and three.”
Our own investigations, however, show a less dramatic influence of water vapor. One aspect is that, similar to CO2, also the water lines are already strongly saturating over wider spectral regions. Therefore, with increasing vapor concentration only the far wings of these lines and weak absorption bands can further contribute to an additional absorption, which roughly logarithmically increases with the vapor concentration.
Another aspect is that always both sw and lw absorption have to be considered. Whereas the lw outgoing radiation is more efficiently blocked and thus contributes to a positive feedback, the sw radiation is also more strongly absorbed in the atmosphere, and less of it reaches the surface, which supplies a negative feedback contribution.
Table 9 shows the results of our calculations for the sw absorptivity , the total lw absorptivity (including cloud absorption), and the back-radiated fraction , which, different to our computations in Section 3, for these feedback studies were calculated at a fixed CO2 concentration of 380 ppm, but for three climate zones with different surface temperatures and, thus, also different WV concentrations . While was taken over from Harde , the lw absorptivity and were derived under conditions as described in Section 3.4, assuming a cloud cover of 66%, a cloud altitude of 6 km, and a cloud emissivity of 48% and using MRT lineshapes, which already include the WV continuum. We have used the same global mean cloud cover and height over all zones. For typical expected cloud variations over the zones and comparing this with the case of clear sky we estimate that this simplification results in an error of less than 5%. Variations of the cloud cover with temperature and their feedback effects are discussed in Section 4.3.6. For the actual feedback analyses it is sufficient and even preferential only to consider the total lw absorptivity, which we designate as and which consists of the absorption by GH gases as well as by clouds.
Figure 7 displays the three key parameters , , and as a function of the surface temperature. The red and the blue line as fits to the calculations directly reflect the temperature dependence of the absorptivities, which at constant gas concentrations would have slightly dropped with increasing temperature but due to the dominating growth of the WV concentration results in a net increase. The linear incline is the result of an exponential growth of the WV concentration with temperature due to Clausius-Clapeyron and on the other hand a logarithmic growth of the absorptivities with the vapor concentration due to saturation effects.
The sw and lw absorptivity changes can well be represented by straight lines with the slopesFor clear sky calculations we further use the value = 0.38%/°C (Harde , ()).
The back-radiated fraction (green circles in Figure 7) as a function of the surface temperature can also well be represented by a straight line with the slope While our calculations in Section 3 describe the variations of with the CO2 concentration and also with cloudiness (see Figures 1–4), this graph displays the additional response of on the temperature and the humidity changes. This response is a typical feedback process, which modifies the up- and downwelling fluxes with the surface temperature and, thus, influences the total radiation and energy balance of EASy. Although the main part of this feedback can be traced back to the increasing WV concentration with temperature, another contribution can be induced by changes of the vertical temperature distribution over the atmosphere and, thus, by changes in the lapse rate. Since it is not advisable to further split these contributions, the temperature dependence of as a whole will be considered in more detail in the next subsection as lapse rate feedback.
Now, taking advantage of (12) and (13) the WV feedback can directly be integrated in our model. This is realized by an iterative procedure, which has been explained in more detail elsewhere (Harde-2014 , Section , pp. 26-27). In a first step the temperature deviation from the reference temperature , caused by a deviation of CO2 from the reference concentration (here 380 ppm), is calculated. This -offset is used to compute with (12) and (13) the corrections in the absorptivities. With the new values again corrected temperatures are determined, which give new absorption corrections. This is repeated, until the temperatures show self-consistency.
The result of such a calculation with WV feedback is illustrated in Figure 8, showing the temperature increase of and as a function of the CO2 concentration. At clear sky (Figure 8(a)) the climate sensitivity rises up from = 1.79°C to 2.81°C, which results in an amplification factor due to the WV feedback of 1.57, or in terms of the feedback parameter (see (9)) gives = 1.10 W/m2/°C. At global mean cloud cover (Figure 8(b)), however, only increases from 1.09°C to 1.24°C, corresponding to an amplification of 1.14 or to a feedback of = 0.43 W/m2/°C.
Compared to AR5-WG1-Tab.9.5, where the WV feedback is specified as a model mean of = W/m2/°C (corresponding to an amplification factor of two), this is a significant discrepancy, even to our clear sky result.
The reasons for this discrepancy are manifold. So, as already mentioned, our calculations also consider the sw absorptivity, which causes a negative feedback, while this is not clear for the feedbacks specified in AR5. The main differences, however, go back to the procedures applied to determine the changes of or with temperature, independent of any variations in . This can best be retraced considering the most important contributions, which are responsible for these changes.
Quite generally we can distinguish two effects and write with as the partial derivative describing the lw (total) absorptivity changes as a function of the water vapor concentration , as the changes of with the surface temperature, as the absorptivity changes with the lw absorption cross-section , and ∂ as the changes of the cross-section with temperature. So, the first term in (15) describes the growth of or with the vapor concentration, which on its own is strongly temperature dependent due to the Clausius-Clapeyron equation; the second term represents the variations of with the absorption cross-section, which changes due to temperature dependent population densities of the involved molecular states and the linewidths (for details see, e.g., Harde-2013 ).
The partial derivative can be found by calculating the absorptivity as a function of the WV concentration and then taking the slope to this curve at a given concentration. Figure 9 displays the lw absorptivity only of water vapor at clear sky via the concentration (lower graph, black diamonds) and on the other hand the total absorptivity (blue squares) resulting from all GH gases and the clouds. Both graphs were calculated applying an MRT lineshape and in the latter case assuming the global mean cloud cover of 66%, an altitude of 6 km, and an emissivity of 0.48. The pink lines are fits to the absorptivities with logarithmic progression.
In this context it has to be mentioned that the absorptivities, reflecting integrals of the absorption coefficients and, thus, integrals of the cross-sections over the altitude and over the spectral distribution (see Harde-2014 , (2–4)), inherently include the general temperature dependence of the absorption coefficients with altitude, but this has to be distinguished from the surface temperature variations, which influence the whole vertical temperature distribution over the atmosphere and which are represented by the second term in (15). The decrease in the WV absorptivity at an increasing ground temperature from 16 to 21°C at otherwise same conditions is represented by green triangles in Figure 9 for three WV concentrations.
In AR5-WG1-Chap.8.3.1 we can read that most intercomparison studies of the RF of GH gases are for clear sky and aerosol-free conditions, while the introduction of clouds would greatly complicate the targets of research and are usually omitted in the intercomparison exercises of GCM radiation codes and LBL codes. Therefore, obviously also for an assessment of the WV feedback cloud effects were neglected. In addition, most of the GCMs emanate from a mean WV concentration of 7,750 ppm, in agreement with the US Standard Atmosphere 1976, representing mid-latitude but not global mean conditions. The slope to the clear sky WV absorptivity at 7,750 ppm then gives = 0.0018%/ppm, and a WV increase of 7%/°C, as assumed in AR5-WG1-FAQ-8.1, contributes to ∂ = 542 ppm/°C. Substituting by this gives for the first term on the right side of (15) the following:and is almost exactly the absorptivity change per °C, necessary to deduce a WV feedback of = 1.6 W/m2/°C and an amplification factor of two, as published in AR5.
So, under these assumptions the IPCC data can well be reproduced. But as outlined above, this approach omits clouds, emanates from a lower WV concentration, and neglects any surface temperature dependence of the absorption cross-section of the GH gases.
Our own considerations include a spectral overlap and interference of WV with other GH gases as well as with clouds, and we assume a global mean WV concentration (at standard conditions) of 14,615 ppm. Both aspects contribute to a larger total absorptivity , but to a reduced pitch around the mean WV concentration and result in a slope = 0.00042%/ppm. Together with a WV increase of 5.9%/°C (see above), which due to the higher WV concentration now contributes to a gain per °C of ∂ = 862 ppm/°C, this gives for the first term in (15) an increase of the total absorptivity of .
The temperature variation of via the absorption cross-section can be found by calculating the absorptivities for different surface temperatures at otherwise identical vapor and gas concentrations. Since for these calculations we assume a fixed temperature at the tropopause of 216.6 K, independent of the surface temperature, any -variations fade with altitude and, thus, also the respective absorptivity changes fade. Therefore, such calculations rather give a lower limit for these changes, yielding a temperature dependence of = −0.08%/°C. Inserting this value for the 2nd term in (15), this contributes to a total lw absorptivity change with temperature of which exactly reproduces the result of (13) and was already derived from the slope of Figure 7.
The direct comparison of the different approaches clearly shows the different assumptions and their influence on the WV feedback. Whereas our result only contributes to an increase of the direct CO2 influence (basic climate sensitivity) of 14%, the IPCC follows from a gain of 100%, which is more than 7 times larger than our result.
4.3.2. Lapse Rate Feedback
The average temperature decrease with altitude over the troposphere is specified as 6.5°C/km and assumed to be constant up to the tropopause at about 11 km altitude . This lapse rate has a direct influence on the power, which is asymmetrically reradiated by the atmosphere in downward and upward direction. In our radiation transfer calculations (see Section 3) this asymmetry is expressed by the parameter , for which at the standard lapse rate we find a back-radiated fraction of about = 62% and a rejected portion to space of () = 38%, slightly varying with the individual assumptions like cloud cover, lineshape, or humidity in an RT calculation. When the vertical temperature profile changes and/or the back-radiation varies due to concentration changes of the GH gases with the temperature, as a direct consequence also the radiation balance will be modified. This induces a climatic effect, known as lapse rate feedback.
It is well known that the tropopause height is significantly varying with the climate zone (also over the seasons) and in so far directly related to the local ground temperature. A detailed description of the tropopause altitude and its variation with latitude has been given by Hoinka . While the mean absorption and reradiation over some longer or shorter distance in the troposphere will not noticeably be influenced, as long as the optical depth is the same, changes of the lapse rate with the ground temperature directly affect the back-radiated fraction and, thus, the total balance of EASy. However, due to dominating wet-adiabatic convection in the atmosphere the lapse rate can be expected to a large extent to be the same even at strongly varying surface temperatures. Nevertheless, a remaining variation of with temperature can be observed which is induced by the stronger WV changes with the climate zone and thus with the surface temperature. The green line in Figure 7 displays this variation of with the ground temperature for the case of a constant lapse rate over the three climate zones as well as over the troposphere and supposing a vertical WV distribution in agreement with the Clausius-Clapeyron-equation. Under these conditions we find a temperature dependence of = 0.11%/°C as already specified in (14), which on its own would contribute to a positive lapse rate feedback of .
On the other side in AR5 we can read “both theory and climate models indicate that global warming will reduce the rate of temperature decrease with altitude, producing a negative lapse rate feedback that attenuates the greenhouse effect.”
So, global circulation models predict an enhanced warming in the upper troposphere of tropical regions, particularly in response to an increasing water vapor concentration, which should result in a negative feedback. On the other hand, at mid- to high-latitudes, a larger low level warming is expected as response to the positive radiative warming, thus, providing a positive feedback, as this is expected from the previous considerations. Since the influence of the tropics is assumed to dominate, in AR4 a resulting negative feedback of −0.85 W/m2/°C was predicted [26, 57], which now has been reduced to (AR5-WG1-Tab.9.5). In our accounting scheme this corresponds to temperature dependence of the back-radiated fraction of = −0.078%/°C and is represented in Figure 7 as magenta line.
Since the water vapor has a more or less stronger influence on the lapse rate, both effects are often considered together. For the combined feedback we then find with an attenuation of 0.95, while the IPCC specifies a value of with an amplification of the climate sensitivity of 1.47 (AR5-WG1-Chap.9, not differentiated between clear sky or cloudiness).
4.3.3. Surface Albedo Feedback
It is well known that changes to the physical properties of the land surface and sea ice will perturb the climate, both by exerting an RF and by modifying other processes such as the fluxes of latent and sensible heat or the transfer of momentum from the atmosphere. Also the other way round is climate influencing the surface properties, which again act back on the climate. So, an increasing ground temperature reduces the Earth’s reflectivity via melting ice shields in the polar regions and it changes the vegetation. With varying reflectivity particularly the sw radiation balance will be modified in such a manner that with reducing sw reflectivity more power is absorbed by the Earth’s surface which then contributes to an additional heating of the ground.
This surface albedo influence is estimated as a positive feedback of = W/m2/°C (AR5-WG1-Tab.9.5). In our simulations we introduce this albedo feedback as a temperature dependent change of the Earth’s reflectivity withwhich under clear sky contributes to an increase of the climate sensitivity of 12% and at mean overcast of 10%.
4.3.4. Convection Feedback
Sensible heat represents the energy transfer through thermal conduction and convection from the warmer surface to the colder atmosphere. At the reference CO2 concentration of 380 ppm and temperature = 16°C this heat flux was chosen to be 17 W/m2 in agreement with the TFK-scheme, and this flux was assumed to be constant in the previous simulations. However, the driving force for this flux is the temperature difference at the boundary layer between surface and atmosphere. In addition, advection in form of a horizontal energy transfer along the boundary through wind and water currents takes place. This transfer is only indirectly dependent on the temperature difference; therefore, it is close-by to assume a power transfer per surface area, which is represented by a temperature independent portion and a temperature dependent part in the formwith as the heat transfer coefficient and as the air temperature at the convection zone.
Since in first approximation can be assumed to scale synchronously with the lower atmospheric temperature , typically reflecting a temperature equivalent to an air layer temperature in about 800 m altitude, but convection is only dominant over about 200 m height, the temperature difference () in (19) is considered to be just one-quarter of the difference () (see Harde-2014 , Subsections and 5.4.4).
Due to the second term in this equation any changes in the surface and atmospheric temperature, which may be induced by CO2, initiate a feedback on EASy. We call this convection feedback.
From Figure 6(a) we see that under clear sky the air temperature reacts less sensitively to CO2 variations than the Earth temperature, and the difference () increases with rising CO2 concentration. Therefore, also the sensible heat flux grows with the concentration and contributes to an additional cooling with a negative feedback.
This feedback gets maximum, when the first term on the right side of (19) vanishes and the total heat flux of 17 W/m2 at 380 ppm CO2 is determined by the second term. Under regular cloud cover with a temperature difference () = 5.2°C the heat convection coefficient can assume a maximum value of = 17/0.25/5.2 = 13 W/m2/°C. When choosing a smaller convection parameter, this automatically reduces the feedback but increases the first term in (19), so that at the reference CO2 concentration always a sensible heat flux of 17 W/m2 is guaranteed (for clear sky it gets slightly larger).
With = 13 W/m2/°C we calculate at clear sky a climate sensitivity of = 1.68°C with a feedback of = −0.19 W/m2/°C and an attenuation factor of 0.94, whereas at regular cloud cover the sensitivity turns into = 1.07°C with a feedback of only = −0.06 W/m2/°C and a damping factor of 0.98. With a more moderate convection coefficient of 4–6 W/m2/°C, as this has to be expected, when some larger fraction of the sensible heat transfer has to be assigned to advective processes, convection feedback still further decreases, and with a damping of less than 1% then this feedback process can well be neglected.
4.3.5. Evaporation Feedback
Latent heat describes the energy transfer resulting from phase transitions of evaporating water or sublimating ice at the surface and their subsequent release of the vaporization energy in the atmosphere, when the water vapor condenses and falls back as precipitation. Similar to sensible heat but even more pronounced this contributes to cooling of the surface. Since an increasing Earth temperature further forces these processes, they also result in a negative feedback, which we call evaporation feedback. Although in more general terms this is also one part of convection, we further distinguish convection and evaporation feedbacks to assign them to sensible and latent heat contributions.
Generally, according to Kirchhoff’s equation (see, e.g., Salby , p. 123) changes in latent heat are directly proportional to temperature changes with a proportionality factor, given by the difference of the specific heats in the two phases. To allow some smaller deviations from this general response over a wider temperature interval, and on the other hand to express only changes in latent heat around a point of reference, as this is of particular interest for our considerations, we assume a similar relationship for latent heat as applied for sensible heat withconsisting of a temperature independent contribution , and a second term proportional to the surface temperature above the freezing point (). is the latent heat transfer coefficient. Under regular conditions almost vanishes, and the feedback, only determined by the second term in (20), gets maximum. Since the total flux at the reference CO2 concentration of 380 ppm is held fixed to 80 W/m2 in agreement with the TFK-scheme, at mean cloud cover can assume a maximum value of 5 W/m2/°C (80 W/m2 ÷ 16°C), which may also be used under clear sky conditions. When for some reason the heat transfer is less sensitively responding to temperature changes (e.g., less rapidly increasing precipitation rate or saturating evaporation), and by this the feedback can slightly decline. Then, in the same way, as the second term in (20) decreases, the first term increases.
At clear sky and maximum = 5 W/m2/°C we find a climate sensitivity of = 1.06°C, a feedback of = −2.1 W/m2/°C, and a damping coefficient of 0.59; at mean cloud cover reduces to = 0.61°C with a maximum negative feedback of even = −2.76 W/m2/°C and a damping of 0.56. So, latent heat can contribute to significant negative feedback and work as a strong stabilizer for the climate.
Similar results for the convection and evaporation feedback were derived by Andrews et al. , who investigated the regression of changes in annual-mean global mean surface heat fluxes against annual-mean global mean for the first 20 yr after CO2 was doubled. As an ensemble mean of various GCMs they specify for the sensible heat feedback (here ) a slightly positive value of 0.26 W/m2/°C and for the latent heat feedback (here ) a stronger negative value of −2.22 W/m2/°C. However, it is not clear how these data were deduced, for clear sky or cloudy conditions.
4.3.6. Thermally Induced Cloud Feedback
Clouds respond to climate forcing mechanisms in multiple ways, and differences in cloud feedbacks constitute by far the primary source of spread of both equilibrium and transient climate responses simulated by climate models (Dufresne & Bony ). So, in AR5-WG1-Chap.7 we can read as follows: “the sign of the net radiative feedback due to all cloud types is less certain (than the net feedback from water vapor and lapse rate changes) but likely positive. Uncertainty in the sign and magnitude of the cloud feedback is due primarily to continuing uncertainty in the impact of warming on low clouds. We estimate… the cloud feedback from all cloud types to be +0.6 (−0.2 to +2.0) W m−2°C−1. These ranges are broader than those of climate models to account for additional uncertainty associated with processes that may not have been accounted for in those models.”
Indeed quite contradictory observations of could effects can be found in the literature, where on the one side regional meteorological conditions over the Pacific are reported, providing modelling evidence for a positive low level cloud feedback in this region on decadal time scales (Clement et al. ). On the other side, particularly in the tropics, the opposite trend is observed that with increasing temperature and thus rising humidity also the cloud formation is increasing, which then contributes to negative feedback (Lindzen et al. ; Laken & Pallé ; Cho et al. ; Caldwell et al. ).
Different to any detailed investigations, which are focusing on individual contributions of low- or high-level clouds to a feedback, here we concentrate on a more general description, how such a feedback can be derived and quantified from global cloud observations and how it can be incorporated into a climate model. Cloud feedbacks can have different origin and importance, depending on the individual forcings, which are responsible for a rebound on the climate via clouds. In this subsection we look closer to CO2 as the responsible climate driver, which initiates a temperature increase and might induce a temperature induced cloud feedback (TICF). In Section 5 we additionally investigate the solar influence on clouds and call this solar induced cloud feedback (SICF).
Our preceding simulations, which were performed for clear sky and at cloudiness, already demonstrate the dominant influence of the clouds as part of the total atmospheric convection on the global temperature and the self-adjusting fluxes between the surface, the atmosphere, and space. So, the climate sensitivity drops to about 60% of its value it had at clear sky conditions, and the ground temperature approximately changes from 20 to 16°C, when the cloud cover increases from 0 to 66%. This temperature response was adopted from the ISCCP observations of the global warming and mean cloud cover variations over the period 1983–2010 , and this response is also the basis for our further assessment of a temperature induced cloud feedback.
It is obvious that the observed temperature changes will not exclusively result from cloud variations or vice versa but will also be affected by variations of the solar radiation, the humidity, or internal oscillations. Therefore, the worst case will be to attribute any response of the cloud cover , as derived from the ISCCP data, only to the surface temperature change Δ and to address this change only to the CO2-GH effect (CO2 induced cloud feedback), this at least around the mean cloud cover of 66% and the mean global temperature of 16°C. Since even at very high temperatures clouds will not completely disappear, we suppose a rest cloudiness of = 20% and an exponential approach to this lower limit. Further, to represent the cloud cover also for negative Δ’s, as this is the case for smaller CO2 concentrations than the reference at 380 ppm, we use for reasons of uniqueness the same functional relation. So, we express the cloud cover as a function of the ground temperature as (see Harde-2014 , ()):with = 66% as the mean cloud cover at = 16°C and as the temperature induced cloud cover parameter. In principle (21) just describes the reciprocal dependence as used in our two-layer model to derive the ground temperature variation as a function of the cloud cover. It is clear that for too large negative temperature deviations would get larger than 100% and then has to be truncated, but within regular variations this is not the case.
To reproduce the cloud variations in agreement with the ISCCP observations, a cloud cover parameter of = 5.4 is required, yielding a cloud cover change of −1% at Δ = 0.065°C. A simulation with this value at mean cloudiness and assuming changes only caused by the CO2-GH effect gives an equilibrium climate sensitivity of ECS = = 2.53°C, corresponding to a feedback = 2.0 W/m2/°C and an amplification of 2.3. With this worst case calculation we can just confirm the upper limit for the cloud feedback as estimated by the IPCC (see above). At the same time, however, this result also makes clear that for a reliable assessment of the climate sensitivity particularly reliable data about the driving force and size of any cloud cover changes are important, since they have an exceptionally strong influence on the further conclusions.
In this context it is important to note that a larger assumed temperature response of the model to cloud changes, as this follows from an inverse scatter plot based on the BEST temperatures, has no influence on the feedback parameters and the climate sensitivities, since due to the reciprocity a larger temperature response of the model is compensated by a smaller cloud cover parameter and vice versa. Only when this reciprocity would not exist, as this might be inferred from the direct plot of the cloud fraction versus BEST temperature with cloud changes of only −3%/°C, would reduce to 1.05, which in our model just reproduces the mean cloud feedback of = +0.6 W/m2/°C as specified in AR5.
In any case, this distinctly lower feedback therefore indicates that obviously(i)the observed cloud changes cannot exclusively be traced back to global warming by CO2, but additional overlaying temperature variations or counteracting processes are present and/or(ii)the cloud changes are additionally or alone controlled by a further climate forcing mechanism.We will come back to these aspects in Section 5.
4.3.7. Total Feedback
The main results of our simulations for the individual and collective feedbacks with their effect on the climate sensitivity are listed in Table 10. The upper 10 lines show the data calculated under clear sky conditions and the 14 lower ones the results under mean cloud cover. Comparison of respective rows without and with overcast clearly demonstrates the dominant influence of clouds, causing a significant reduction of the sensitivities, as long as the thermally induced cloud feedback is excluded. So, with water vapor, lapse rate, albedo, and evaporation feedback diminishes to 0.62°C (line 22).
Additionally assuming CO2 induced cloud feedback with a cloud cover parameter = 5.4 and a medium convection feedback ( = 5 W/m2/°C) the climate sensitivity rises to = 1.22°C, and the previously observed reduction, compared to clear sky, is almost lost (compare lines 10 and 24). The same mechanism, which reduces the temperature with increasing cloud cover, is also active in opposite direction.
It is also worth noting that with an increasing negative evaporation feedback the convective part, which under mean cloudiness is already quite small (see line 15), is still further pressed down and under special conditions even can get slightly positive. In general, however, when a moderate heat convection coefficient is chosen to allow also advective heat transfer, a convective feedback can completely be neglected. From this behavior we also see that the total feedback is by far not only the sum of the individual contributions.
Due to the above assumptions that the observed cloud changes within the ISCCP program are only thermally induced and the respective temperature increase over this period is only caused by CO2 (maximum cloud feedback = 2.0 W/m2/°C), our analysis with all the other feedbacks included shows that a climate sensitivity of = 1.2°C obviously represents an upper limit for this quantity. Similar conclusions hold for the response of EASy with a ground temperature variation of 7°C at a 100% cloud cover change. Obviously also paleo-climatic investigations (see, e.g., Petit et al. ) indicate that EASy stabilizes itself within temperature variations of about 6-8°C, and this still under the influence of even much stronger solar changes as well as under much larger CO2 concentrations, as they were found 500 Mio years ago.
With a cloud response of = 1.05 ( = +0.6 W/m2/°C, see line 23) the climate sensitivity assumes a moderate value of = 0.74°C. Under these conditions the observed warming over the last hundred twenty years of about 0.8°C, which the IPCC almost exclusively assigns to anthropogenic forcing, could only be explained to less than one-half (0.31°C) by the 100 ppm CO2 increase over this period. That is, most of the observed warming could not follow from anthropogenic forcing. If the warming over the eighties and nineties additionally might have been superimposed by some other thermal processes, for example, an increased solar activity, Pacific Decadal Oscillations (PDO), the Southern Oscillation Index (SOI), or other GH gases, the respective CO2 initiated contribution to cloud changes further diminishes, which also reduces the feedback and in the same way the climate sensitivity.
As direct comparison to our calculations we have also listed a simulation assuming the feedbacks as used in AR5-WG1-Tab.9.5 with a WV plus lapse rate feedback of = 1.1 W/m2/°C, ( = 0.98%/°C, = = −0.08%/°C), an albedo feedback of = 0.3 W/m2/°C ( = −0.143%/°C), and a cloud feedback (see AR5-WG1-Chap.7) of = 0.6 W/m2/°C ( = 1.05). With these parameters we find a climate sensitivity of = 2.9°C, which is 10% smaller than the model mean of the CMIP5 AOGCMs and essentially results from our smaller Planck sensitivity (see Table 8), but otherwise reproduces the AOGCMs very well. So, the big discrepancy between the IPCC’s accounting scheme and ours can clearly be identified to originate from the negative WV lapse rate feedback and the negative evaporation feedback considered in our calculations.
Altogether, we see that the dominating positive feedbacks, originating from clouds and albedo, are partially compensated or in the case of a moderate cloud feedback are even overcompensated by negative WV lapse rate and evaporation feedback. Particularly clouds have two stronger opposing influences on the energy balance, which can neutralize each other or can even have an overall attenuating impact on the ECS, dependent on the mechanisms responsible for cloud changes.
So, up to now it is not clear if the ISCCP observations are really only a consequence of the increased temperature as assumed in Section 4.3.6 or at least to some degree are stimulated by nonthermal solar activity over the observation period (Ziskin & Shaviv ; Vahrenholt & Lüning ; Svensmark et al. [23, 65, 66]; Enghoff et al. ; Kirkby et al. ). In the latter case the strong thermal cloud feedback had to be cancelled with the effect that at otherwise same conditions the climate sensitivity would drop to about 0.6°C.
An important criterion for a serious validation, which mechanism really might control the cloud cover changes, we can derive from model simulations, which additionally include the solar anomaly over the last century and compare this directly with the observed global warming over this period. Similar investigations have been performed by Ziskin and Shaviv , where they show that obviously such solar induced component is necessary to reproduce the 20th century global warming and that the total solar contribution is much larger than can be expected from variations of the total solar irradiance (TSI) alone.
To verify the existence and size of such a solar effect in the total energy budget we have performed quite similar analyses, which also include solar variations and orientate at the observed warming over the last century, but which are based on our two-layer model, including all discussed feedback processes and especially reproducing the ISCCP observations of cloud cover changes. Of course, any conclusions deduced from such comparison sensitively depend on the reliability of the measured cloud cover, the solar activity, and temperature changes over this period.
5. Solar Influence
In the same way as the GH gases have an influence on the radiation and energy budget of EASy, this is the case for a varying solar activity. Both are external perturbations, causing an imbalance, to which EASy has to respond with a new distribution for the respective temperatures at the surface and in the atmosphere.
Such response on a varying solar activity can easily be simulated with our two-layer climate model by changing the solar constant (total solar irradiance, TSI) or the average solar flux in our parameter list in Table 6. So, a simulation with a 0.1% larger TSI contributes to an increase of the surface temperature of 0.09°C. In analogy to the CO2 climate sensitivity we may call this the solar sensitivity . Typically, over a Schwabe cycle (11 years) variations of the solar constant of 0.1–0.12% are observed, corresponding to an equilibrium temperature change of about 0.1°C.
But for a serious assessment of the solar influence on global warming we further have to discuss two contributions, which can modify the basic solar sensitivity :(i)an amplification by a possible temperature induced cloud feedback, which works in the same way as discussed for the CO2 induced cloud feedback but now results from the solar heating, and(ii)a temperature independent mechanism, which acts back on the cloud formation when the solar activity is changing and in this way contributes to an amplification of . We call this a solar induced nonthermal cloud feedback.We first look to their individual contributions before we unify them in a common model which orientates at the global warming over the last century and allows an assessment of the influence of the two climate drivers, the CO2, and the Sun, on our climate.
5.1. Thermally Induced Cloud Feedback
When a thermally induced cloud feedback (TICF), as discussed in Section 4.3.6, is assumed to be responsible for the observed cloud cover changes, this feedback also has to be applied to the direct solar initiated warming. Here we focus only on CO2 and solar induced contributions, while other effects caused by internal oscillations or volcanic activities are neglected. For the climate and solar sensitivity this should rather give an upper limit. Their individual contributions and, therefore, their relative weighting can be derived, comparing the CO2 fraction with the respective solar part, including all feedback processes.
With a thermal cloud response of = 5.4 and for 100 ppm CO2 increase we calculate a maximum temperature growth of 0.52°C corresponding to a climate sensitivity of = 1.22°C. The solar part can be assessed from an analysis of Shapiro et al.  of long-term solar activity proxies over the last century, which shows an increase of the TSI of slightly more than Δ = 0.3% in good agreement with the observed decadal group sunspot numbers over this period (see Hoyt & Schatten , updated by Scafetta & Willson ). These results are remarkably well confirmed by a new adjustment-free physical reconstruction of solar activities (Usoskin et al. ), which indicates a modern Grand maximum (during solar cycles 19–23, that is, 1950–2009) and is found to be a rare or even unique event, in both magnitude and duration, in the past three millennia. Also an actual composite by Soon et al.  of the Northern Hemisphere temperature trend, which is mainly based on rural data, supports a stronger influence and variation of the TSI over the last century. So, assuming a solar anomaly of Δ = 0.3% this donates a temperature increase of 0.31°C, which in this case corresponds to a solar sensitivity of = 0.1°C. The relative contributions of CO2 and the Sun then behave as about 60 to 40%.
Both together give a warming over the last century of 0.83°C which is slightly more than the observed temperature boost over the last 120 years of 0.74°C (GISS ). Although meanwhile the IPCC emanates from a larger global warming of 0.85°C, we refer to the original value of , which is in good agreement with the single longest dataset available, yielding a total increase between the average of the 1850–1900 period and the 2003–2012 period with 0.78°C (AR5-WG1-SPM). From Soon et al.  we even deduce an increase over the last century of only slightly less than 0.7°C.
Only with a reduced solar anomaly of Δ = 0.22%, yielding a solar contribution of 0.22°C, or also with a further increased negative feedback the temperature balance could again be satisfied. Without the negative evaporation and convection feedbacks the warming would be completely unrealistic with 1.6°C for CO2 plus 1.2°C for solar heating. So, well knowing that the observed warming does not represent an equilibrium state, different to our calculations, and can further be superimposed by other effects like the PDO and SOI (see, e.g., Spencer & Braswell ), it looks like that a thermal cloud feedback of = 2 W/m2/°C ( = 5.4) appears too high.
On the other hand using a cloud feedback as assumed by the IPCC with = 0.6 W/m2/°C ( = 1.05) the CO2 contribution declines to 0.31°C and the solar part to 0.17°C. Then their sum is too small to explain the observed warming. However, in any case is such reduced thermal cloud feedback no longer in agreement with the observed cloud changes. As a consequence we state the following: either a maximum thermal cloud feedback of = 2.0 W/m2/°C ( = 5.4) has to be assumed, this at a reduced solar anomaly and/or a further increased negative feedback, or at least some fraction of the cloud cover is also influenced by nonthermal cloud cover changes.
5.2. Solar Induced Cloud Feedback
Since the amount of clouds varies over the solar cycle, there exists strong evidence that the solar activity variations also modulate the cloud cover. Actual publications of Svensmark [23, 65–67] indicate that with an increasing solar activity and, therefore, an increasing solar magnetic field the cosmic flux, which hits the atmosphere, is reduced and causes a direct feedback on the cloud cover. So, it is expected that the generation rate of aerosols as condensation seeds for the formation of water droplets in the lower atmosphere is directly influenced by the cosmic radiation flux (see also cloud experiment, Kirkby et al. ), which therewith also controls the cloud cover.
Another proposed mechanism is hypersensitivity of the climate system to ultraviolet (UV) radiation, which typically varies 10x stronger over a solar cycle than the TSI (Haigh [24, 71]; Soon et al. ; Haigh et al. ). So, increased UV radiation activates the stratospheric ozone production and heat transfer, which via atmospheric waves can further induce sea surface temperature and/or tropospheric circulation variations and in this way also modulate the cloud cover (Kristjánsson et al. ).
Obviously both these mechanisms play a role, depending on the climatic conditions and altitude (Voiculescu et al. ). Due to their close interrelation here we consider them as a unique effect.
A reduced cloud formation at an increased solar activity then reinforces the initial TSI induced temperature increase and can be included in the 2LCM as a feedback term similar to the thermally induced cloud changes, but now depending on changes of the solar constant, supposing that variations in initiate reciprocal changes in the cloud cover with (see Harde-2014 , 86):where is the mean solar constant as a reference and the solar induced cloud cover parameter.
Assuming that the cloud cover variation over the period 1983–2000 of −4% is only determined by an observed increase of the TSI of = 0.1% (Willson & Mordvinov ), this results in a feedback parameter = 90. It should be noticed that a smaller supposed increase of the TSI over this period (designated as ) and therefore deviating from Willson & Mordvinov only pushes the parameter further up and increases the solar feedback.
With this additional solar induced cloud feedback (SICF) the basic solar sensitivity of 0.09°C rises to = 0.31°C. However, in the same way as any warming causes further feedback processes, as discussed in Section 4.3.7, also warming according to solar stimulated cloud changes will further be amplified or attenuated. With all feedbacks included in this case we find a solar sensitivity of = 0.18°C, which then replaces the previously specified value, derived under conditions of TICF.
When SICF is the only responsible process controlling the cloud cover, also for the CO2 climate sensitivity TICF has to be cancelled and reduces to 0.66°C.
With a solar anomaly of Δ = 0.3% and a solar sensitivity of = 0.18°C this already gives a temperature increase of 0.51°C (slightly nonlinear), which is 0.2°C more than the solar contribution for pure TICF (see Section 5.1). On the other hand CO2 with an increase of 100 ppm over this period (and applying the respective climate sensitivity of = 0.66°C, now without TICF) then only delivers additional 0.28°C. The sum with 0.79°C again gives a slightly too high growth over the last 120 years. However, with a smaller solar anomaly, in this case of 0.27% over this period, the warming can exactly be reproduced. Under these conditions the Sun contributes 69% to global warming and CO2 the rest.
Similar to Shapiro et al. , Hoyt & Schatten , Scafetta & Willson , Usoskin et. al. , and Soon et al.  a larger solar influence on global warming has also been reported by Zhao and Feng , who have investigated the periodicities of the solar activity and the Earth’s temperature variation on a time scale of centuries, using the wavelet and cross correlation analysis techniques. From this they conclude that during the past 100 years solar activities display a clear increasing tendency which correlates very well with the global warming of the Earth, including land and ocean.
If the solar anomaly (related to the last century) should have been overestimated and would only be Δ = 0.1% (see Wenzler et al. ), it has to be expected that also is declining, for example, to 0.05%. Then, with = 180, the solar fraction still contributes more than 50% to global warming.
Here we do not discuss any additional influence of aerosols over this period, since any reliable figure of such effect is largely unknown and is not the subject of feedback processes. Implicitly aerosols are already enclosed in our model via atmospheric and cloud backscattering, so that any aerosol impact could easily be modelled by varying the sw backscattering parameters and if necessary also the cloud absorption.
5.3. Combined Solar and Thermally Induced Cloud Feedback
The previous investigations have made clear that the measured cloud cover changes by the ISCCP cannot satisfactorily be explained by a pure thermal mechanism. Either this gives too high global warming over the last century, or with the IPCC’s favored cloud feedback it results in a too small cloud cover variation over the eighties and nineties. Also a pure solar induced nonthermal cloud feedback with a solar anomaly of Δ = 0.3% results in a slightly too high global warming. So, in both cases, some smaller corrections in the solar variability and/or the total feedback would be necessary to satisfy all constraints.
On the basis of our investigations reasons for a still stronger negative feedback are not so much expected, although we always assumed a more conservative assessment, for example, excluding an internal variability with its influence on the global temperature and cloud effects. This would even further increase the discrepancy to the IPCC’s assessment of the ECS. However, larger uncertainties exist for the solar anomaly over the last century and its influence on cloud cover changes. Since the size of this anomaly has far reaching consequences on both cloud changing mechanisms, it is necessary to consider this influence in more detail, and as long as it is not clear which of these mechanisms is the dominating feedback process it is even reasonable to discuss a combination of these effects.
One way to handle the simultaneous presence of TICF and SICF is to modify the thermal and the solar induced cloud cover parameters and which then determine the weighting of a mechanism relative to their maximum values. The other possibility is to leave the cloud parameters fixed at their predetermined values for a cloud cover change in agreement with the observations and then directly weighting the two feedback processes, which together have to satisfy the constraints for global warming and cloud cover changes. Both procedures give similar results, but the second appears more straightforward and was preferred in our further simulations. The principal accounting scheme can be retraced from Figure 10.
First the weighting factor for the thermal to solar feedback has to be calculated, which specifies an additional admixture of the thermally induced cloud cover changes to the solar initiated changes, this with the objective to satisfy the warming balance over the last century. This weighting should not be mixed with the fraction of the CO2 initiated to the solar created warming, which can finally be derived as one important result of this calculation model. The weighting requires determining the temperature at 380 ppm CO2 with increased TSI (), then at 280 ppm and regular TSI (), both for = 0 and = 90 (only solar induced) and including all other feedbacks. Their difference gives the total warming caused by CO2 and the Sun under conditions with only the nonthermal SICF present (see Section 5.2). The same procedure is repeated for = 5.4 and = 0, yielding the total warming caused by CO2 and the Sun with only TICF active (Section 5.1). The difference between the observed warming over the last century = 0.74°C and the nonthermal contribution, this in relation to the difference between thermal and nonthermal contributions, determines the weighting of the thermally induced cloud cover changes. The respective compliment to one gives the solar induced part as follows: Further multiplying the temperature difference between 380 and 280 ppm CO2 at regular TSI ( = 5.4 and = 0) with the thermally induced weighting, then multiplying the respective difference at = 0 and = 90 with the nonthermally induced weighting, and taking the sum of these two products finally gives the CO2 portion to global warming as follows:The equivalent procedure now at fixed CO2 concentration but with the differences between increased and regular TSI gives the solar contribution to global warming as follows:Within regular bounds the sum of the CO2 and solar induced warming then should reproduce the measured warming over the last century, while satisfying the observed ISCCP cloud cover changes.
The respective climate sensitivity is found from the maximum ECS (full TICF) times the thermal weighting, plus the minimum ECS (no TICF) times the solar weighting as follows:The solar sensitivity can be derived from the temperature growth at increasing TSI and with TICF times the thermal weighting, plus the temperature rise due to SICF times the solar weighting and all this normalized to the increased solar activity Δ as follows:
Some typical results based on this combined accounting scheme are compiled in Table 11. All simulations include the previously discussed feedback effects with parameters for the WV, lapse rate, albedo, convection, and evaporation feedback as specified in Table 10, line 24.