Journal topic
Atmos. Chem. Phys., 18, 6317–6330, 2018
https://doi.org/10.5194/acp-18-6317-2018
Atmos. Chem. Phys., 18, 6317–6330, 2018
https://doi.org/10.5194/acp-18-6317-2018

Research article 04 May 2018

Research article | 04 May 2018

# Global warming potential estimates for the C1–C3 hydrochlorofluorocarbons (HCFCs) included in the Kigali Amendment to the Montreal Protocol

Global warming potential estimates for the C1–C3 hydrochlorofluorocarbons (HCFCs) included in the Kigali Amendment to the Montreal Protocol
Dimitrios K. Papanastasiou1,2, Allison Beltrone3, Paul Marshall3, and James B. Burkholder1 Dimitrios K. Papanastasiou et al.
• 1Earth System Research Laboratory, Chemical Sciences Division, National Oceanic and Atmospheric Administration, 325 Broadway, Boulder, CO 80305, USA
• 2Cooperative Institute for Research in Environmental Sciences, University of Colorado, Boulder, CO 80309 USA
• 3Department of Chemistry, University of North Texas, P.O. Box 305070, Denton, TX 76203-5070, USA

Correspondence: James B. Burkholder (james.b.burkholder@noaa.gov)

Abstract

Hydrochlorofluorocarbons (HCFCs) are ozone depleting substances and potent greenhouse gases that are controlled under the Montreal Protocol. However, the majority of the 274 HCFCs included in Annex C of the protocol do not have reported global warming potentials (GWPs) which are used to guide the phaseout of HCFCs and the future phase down of hydrofluorocarbons (HFCs). In this study, GWPs for all C1–C3 HCFCs included in Annex C are reported based on estimated atmospheric lifetimes and theoretical methods used to calculate infrared absorption spectra. Atmospheric lifetimes were estimated from a structure activity relationship (SAR) for OH radical reactivity and estimated O(1D) reactivity and UV photolysis loss processes. The C1–C3 HCFCs display a wide range of lifetimes (0.3 to 62 years) and GWPs (5 to 5330, 100-year time horizon) dependent on their molecular structure and the H-atom content of the individual HCFC. The results from this study provide estimated policy-relevant GWP metrics for the HCFCs included in the Montreal Protocol in the absence of experimentally derived metrics.

1 Introduction

Hydrochlorofluorocarbons (HCFCs) are ozone depleting substances (ODSs), the production and use of which are controlled under the Montreal Protocol on Substances that Deplete the Ozone Layer (1987). HCFCs have been used as substitutes for chlorofluorocarbons (CFCs) in various commercial and residential applications, e.g., foam blowing, and refrigerator and air conditioning systems. In addition to being ODSs, HCFCs are also potent greenhouse gases (WMO, 2014).

With the adoption of the Kigali Amendment (2016) to the Montreal Protocol by the Twenty-Eighth Meeting of the Parties to the Montreal Protocol, parties agreed to the phasedown of hydrofluorocarbons (HFCs), substances that are not ozone depleting but are climate forcing agents. As in the case of HCFCs, the HFC production and consumption control measures comprise reduction steps from established baselines (see UN Environment OzonAction Fact Sheet; UN, 2017), which are different for developed and developing countries with an exemption for countries with high ambient temperature. Since HFCs are greenhouse gases, baselines and reduction steps are expressed in CO2 equivalents. The amended protocol controls eighteen HFCs as listed in Annex F of the protocol.

Although the phasedown steps stipulated in the Kigali Amendment concern only HFCs, the baselines for the reductions are derived through formulae involving both HCFC and HFC production and consumption because HFCs are intended to be substitute compounds for HCFCs. This necessitates knowledge of the global warming potentials (GWPs), a policy-relevant metric representing the climate impact of a compound relative to CO2, of all HCFCs involved in the baseline formulae. However, in the amended protocol, GWPs are available for only eight HCFCs (HCFCs-21, -22, -123, -124, -141b, -142b, -225ca, and -225cb) from a total of 274 HCFCs included in Annex C (274 is the sum of all C1–C3 HCFC isomers). Of the 274 HCFCs, only 15 have experimental kinetic and/or infrared absorption spectrum measurements used to determine their GWPs. The majority of the HCFCs listed in Annex C are not currently in use, but the intent of the protocol was for a comprehensive coverage of possible candidates for future commercial use and possible emission to the atmosphere. For molecules with no GWP available, a provision is included in the protocol stating that a default value of zero applies until such a value can be included by means of adjustments to the protocol. Having policy-relevant metrics for these compounds will help guide and inform future policy decisions.

The objective of the present work is to provide a comprehensive evaluation of the following: atmospheric lifetimes; ozone depletion potentials (ODPs), which represents the ozone depleting impact of a compound relative to a reference compound (see WMO, 2014, and references within); GWPs; and global temperature change potentials (GTPs), another policy-relevant metric representing the climate impact of a compound relative to CO2, for the HCFCs listed in Annex C of the amended protocol. The HCFCs that have experimentally measured OH rate coefficients, the predominant atmospheric loss process for HCFCs, and infrared absorption spectra were used as a training dataset to establish the reliability of the methods used to estimate the metrics for the other HCFCs. The training dataset compounds and reference data are listed in Table 1. In the following section, brief descriptions of the methods used to determine the HCFC atmospheric lifetime and ODP are given. Next, the theoretical methods used to calculate the infrared spectra of the HCFCs are described. The infrared spectra are then combined with our estimated global atmospheric lifetimes to estimate the lifetime and stratospheric temperature adjusted radiative efficiency (RE), GWP, and GTP metrics (see IPCC, 2013; WMO, 2014). In the results and discussion section, a general overview of the obtained metrics is provided, while the details and results for each of the individual HCFCs are provided in the Supplement.

Table 1Summary of hydrochlorofluorocarbon (HCFC) parameters in the training dataseta.

a Lifetimes, RE, and GWP values taken from WMO ozone assessment (WMO, 2014) unless noted otherwise. Where multiple sources for infrared spectra are available, the spectra reported from the NOAA laboratory (McGillen et al., 2015) and the PNNL database (Sharpe et al., 2004) were used in the analysis. b Rate coefficients taken from NASA evaluation (Burkholder et al., 2015) unless noted otherwise. c Rate coefficient and metrics taken from McGillen et al. (2015) with RE lifetime adjusted and a factor of +1.1 for stratospheric temperature correction applied.

2 Methods

The global atmospheric lifetime (τatm) is defined as follows:

$\frac{\mathrm{1}}{{\mathit{\tau }}_{\text{atm}}}=\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{OH}}}+\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{O}{\left(}^{\mathrm{1}}\mathrm{D}\right)}}+\frac{\mathrm{1}}{{\mathit{\tau }}_{h\mathit{\nu }}},$

where τOH, ${\mathit{\tau }}_{\text{O}{\left(}^{\mathrm{1}}\mathrm{D}\right)}$, and τhν are the global lifetimes with respect to OH and O(1D) reactive loss and UV photolysis, respectively. Other reactive and deposition loss processes for HCFCs are expected to be negligible and not considered in this study. τatm is also often defined in terms of its loss within the troposphere (τTrop), stratosphere (τStrat), and mesosphere (τMeso) as

$\frac{\mathrm{1}}{{\mathit{\tau }}_{\text{atm}}}=\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{Trop}}}+\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{Strat}}}+\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{Meso}}},$

where for example,

$\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{Strat}}}=\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{Strat}}^{\mathrm{OH}}}+\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{Strat}}^{\mathrm{O}{\left(}^{\mathrm{1}}\mathrm{D}\right)}}+\frac{\mathrm{1}}{{\mathit{\tau }}_{\mathrm{Strat}}^{h\mathit{\nu }}}$

For the HCFCs considered in this study, mesospheric loss processes are negligible and not considered further. The atmospheric loss processes for the HCFCs considered in this study have not been determined experimentally, while τTrop is predominately determined by the HCFC reactivity with the OH radical. In this work, ${\mathit{\tau }}_{\text{Trop}}^{\text{OH}}$ was estimated using the CH3CCl3 (MCF) relative method (WMO, 2014) where

${\mathit{\tau }}_{\text{Trop}}^{\text{OH}}={\mathit{\tau }}_{\text{OH}}^{\text{HCFC}}=\frac{{k}_{\text{MCF}}\left(\mathrm{272}\phantom{\rule{0.125em}{0ex}}\text{K}\right)}{{k}_{\text{HCFC}}\left(\mathrm{272}\phantom{\rule{0.125em}{0ex}}\text{K}\right)}{\mathit{\tau }}_{\text{OH}}^{\text{MCF}},$

with the MCF recommended rate coefficient, kMCF(272 K) = 6.14 × 10−15 cm3 molecule−1 s−1 (Burkholder et al., 2015), and tropospheric lifetime, 6.1 years (WMO, 2014).

In the absence of experimental OH reaction rate coefficients, a structure activity relationship (SAR) was used to estimate OH reaction rate coefficients. The SAR of Kwok and Atkinson (1995) and DeMore (1996) were compared with the rate coefficients for the 15 HCFCs (training dataset) for which experimental kinetic measurements are available (Burkholder et al., 2015). The DeMore SAR clearly performed better for these halocarbons and was used in this study. Figure 1 shows the agreement between the experimental 298 K rate coefficient data and the SAR predicted values. For the determination of kHCFC(272 K) an ER value of 1400 K was used in the Arrhenius expression, k(T) =Aexp(1400  T), which is a representative value for the HCFC reactions included in Burkholder et al. (2015). On the basis of the training dataset calculations, we estimate the uncertainty in the SAR 298 K rate coefficients to be  30 % on average. The uncertainty at 272 K will, in some cases, be greater due to our assumption that ER= 1400 K for the unknown reaction rate coefficients. A  50 % uncertainty spread encompasses nearly all the training dataset values at 272 K, see Fig. 1. Therefore, we estimate a 50 % uncertainty in k(272 K) for the HCFCs with unknown rate coefficients.

Figure 1Comparison of structure activity relationship (SAR) OH rate coefficients for the training dataset (Table 1) with rate coefficients recommended in Burkholder et al. (2015). (a) Rate coefficients at 298 K using the SAR of DeMore (1996) (solid symbols) and Kwok and Atkinson (1995) (open symbols). The dashed line is the 1:1 correlation and the shaded region is the ±30 % spread around the 1:1 line. (b) Rate coefficients at 272 K using the SAR of DeMore (1996) (solid symbols) with an ER= 1400 K. The dashed line is the 1:1 correlation, the gray shaded region is the ±30 % spread, and the blue shaded region is the ±50 % spread around the 1:1 line.

τStrat for the HCFCs is determined by a combination of OH and O(1D) reactive loss, and UV photolysis. Presently, there is no simple means to determine stratospheric lifetimes without the use of atmospheric models. Here, we have estimated stratospheric OH loss lifetimes, ${\mathit{\tau }}_{\text{Strat}}^{\text{OH}}$, following a methodology similar to that used in the WMO (2014) ozone assessment, where results from 2-D atmospheric model calculations are used to establish a correlation between tropospheric and stratospheric lifetimes. We used the lifetimes taken from the SPARC (Ko et al., 2013) lifetime report for three HCFCs and eight HFCs to establish a lifetime correlation, which is shown in Fig. S1 in the Supplement. The stratospheric loss via the OH reaction accounts for  5 % of the total OH loss process for > 95 % of the HCFCs. Therefore, this method of accounting for stratospheric loss leads to only a minor uncertainty in the calculated global lifetime.

In most cases, O(1D) reaction and UV photolysis are minor contributors to the global loss of a HCFC. In the absence of experimental data, O(1D) rate coefficients were estimated using the reactivity trends reported in Baasandorj et al. (2013). τO(1D) for the HCFCs were based on a comparison with similarly reactive compounds included in the SPARC (Ko et al., 2013) lifetime report. As shown later, the O(1D) reaction is a minor loss process, < 1 %, for nearly all the HCFCs included in this study and, therefore, the estimation method used is not critical as this loss process is a minor contributor to the global lifetime. τhν was estimated based on the molecular Cl-atom content and its distribution within the molecule as follows: each isolated Cl-atom (450 years), each CCl2 group (80 years), each CCl3 group (50 years), with a minimum photolysis lifetime of 50 years (Ko et al., 2013). UV photolysis is a minor loss process, with the exception of a few long-lived highly chlorinated HCFC isomers where photolysis accounts for 15 % of the global loss at most.

A minimum stratospheric lifetime of 20 years was applied to approximately account for transport limited stratospheric lifetimes.

## 2.2 Ozone depletion potentials (ODPs)

Semi-empirical ODPs were calculated using the following formula:

${\mathrm{ODP}}_{\text{HCFC}}=\frac{{n}_{\mathrm{Cl}}}{\mathrm{3}}\phantom{\rule{0.125em}{0ex}}\frac{{f}_{\text{HCFC}}}{{f}_{\mathrm{CFC}\text{-}\mathrm{11}}}\phantom{\rule{0.125em}{0ex}}\frac{{M}_{\mathrm{CFC}\text{-}\mathrm{11}}}{{M}_{\mathrm{HCFC}}}\frac{{\mathit{\tau }}_{\text{HCFC}}}{{\mathit{\tau }}_{\mathrm{CFC}\text{-}\mathrm{11}}},$

where nCl is the number of Cl-atoms in the HCFC; M is the molecular weight; f is the molecules fractional release factor (FRF), which denotes the fraction of the halocarbon injected into the stratosphere that has been dissociated (Solomon and Albritton, 1992); and τ is the global atmospheric lifetime. The fractional release factor and global lifetime for CFC-11 were taken from the WMO (2014) ozone assessment report to be 0.47 and 52 years, respectively. Note that a new method to calculate FRF has been suggested by Ostermöller et al. (2017a, b), which has been applied by Leedham Elvdige et al. (2018) and Engel et al. (2018). Overall, there is good agreement between the new method and the empirical parameterization applied in this work. The fractional release factors for the majority of the HCFCs included in this study have not been reported. The WMO report included 3 year age of air FRFs derived from model studies and field observations for 20 ozone depleting substances (WMO, 2014). In the absence of recommended FRF values, we derived an empirical FRF vs. stratospheric lifetime relationship, shown in Fig. 2, for the compounds with reported FRFs and the 2-D model stratospheric lifetimes reported in the SPARC (Ko et al., 2013) lifetime report. Table S1 provides the values presented in Fig. 2. A fit to the data yielded FRF = 0.06 + 0.875 × exp(0.0144 ×τStrat), which was used in our calculations.

Figure 2Empirical correlation of fractional release factor (FRF) versus stratospheric lifetime, τStrat. Stratospheric lifetimes were taken from 2-D model results given in the SPARC (Ko et al., 2013) lifetime report. The FRFs were taken from WMO assessment (WMO, 2014). The solid line is a fit to the data: FRF = 0.06 + 0.875 exp(0.01444 ×τStrat).

## 2.3 Theoretical calculations

Information about molecular vibrational frequencies, central to the interpretation of infrared spectra, thermodynamics, and many other aspects of chemistry, became amenable to computational determination in the early 1980s. It was recognized that computed harmonic frequencies derived via the second derivative of energy as a function of atomic position were systematically higher than observed fundamentals and scale factors were introduced (Hout et al., 1982; Pople et al., 1981). For Hartree–Fock frequencies these were typically  0.9 and accounted both for the influence of anharmonicity and deficiencies in the underlying quantum calculations. Frequencies based on methods incorporating electron correlation such as CCSD, CCSD(T), or certain functionals within density functional theory (DFT) often perform well for harmonic frequencies and are scaled by  0.95 to match fundamental vibrational modes. Such scaling has been updated as more methods appear (Alecu et al., 2010; Scott and Radom, 1996). Rather less information is available concerning the evaluation of absorption intensities for fundamental modes. Within the same harmonic approximation, implemented in popular quantum codes, the intensity is proportional to the square of the derivative of the dipole moment with respect to position. Halls and Schlegel (1998) evaluated QCISD results against experimental results that indicated deviations of up to approximately ±20 %; they then used QCISD as a benchmark to evaluate a range of functionals. For B3LYP, they found differences from QCISD of around 10 %. More recently, tests of the B3LYP functional found good performance for frequency and intensity (Jiménez-Hoyos et al., 2008; Katsyuba et al., 2013). Some prior work where similar methods have been applied to the infrared absorption for molecules of atmospheric interest include studies of fluoromethanes (Blowers and Hollingshead, 2009), unsaturated hydrofluorocarbons (Papadimitriou and Burkholder, 2016; Papadimitriou et al., 2008b), perfluorocarbons (Bravo et al., 2010), chloromethanes (Wallington et al., 2016), SO2F2 (Papadimitriou et al., 2008a), permethylsiloxanes (Bernard et al., 2017), and large survey studies such as by Kazakov et al. (2012) and Betowski et al. (2015) to name a few.

Halls and Schlegel noted that real spectra may exhibit the influences of resonances, intensity sharing, and large-amplitude anharmonic modes. These can be partially accounted for in an analysis based on higher derivatives of the energy and the dipole moment, performed for instance within the framework of second-order vibrational perturbation theory (Barone, 2005). Advantages include treatment of resonances among vibrational levels and incorporation of overtones and combination bands. Examples of applications to molecules containing C–H and C–F bonds indicate excellent accord with experiments for band position and intensity, (Carnimeo et al., 2013) but for CH2ClF the intensity in the region involving C–Cl stretching nevertheless exhibits intensity errors of  10 % (Charmet et al., 2013).

The large number of molecules considered in this work and the associated geometry optimizations,  1500 optimizations, required that a cost-effective methodology with reasonable accuracy such as DFT methods be used. Geometry optimization and vibrational frequencies for all C1–C3 HCFCs were carried at the B3LYP/6-31G(2df,p) level using the Gaussian 09 software suite (Frisch et al., 2016). Similar approaches have been used in earlier studies for other classes of molecules with good results, see Hodnebrog et al. (2013) and references cited within. The calculations presented in this work included only the 35Cl isotope because the large number of possible isotopic substitution permutations made the calculation of all combinations prohibitive. In principle, substitution of 35Cl by 37Cl in a heavy molecule would lower the frequency of the C–Cl stretch by  3 %. The level of theory was evaluated based on comparison with available experimental HCFC infrared spectra, see Table 1. Note that our calculations and data available in the NIST quantum chemistry database (2016) obtained using a more costly triple-ζ basis set (aug-cc-pVTZ) showed only minor differences in the calculated frequencies, < 1 %, and band strengths, < 10 %, for the molecules in the training dataset.

The majority of the HCFCs have multiple low-energy conformers that have unique infrared absorption spectra. Although only the most stable conformer has been used in most previous theoretical studies, including the individual conformers provides a more realistic representation of the HCFCs infrared spectrum and is expected to improve the accuracy of the calculated radiative efficiency as discussed below. We are not aware of prior studies of infrared spectra of HCFC conformers, but there have been prior theoretical studies of the conformers of other classes of molecule, such as for validation of observed infrared spectra used to deduce relative energies of carbonyl conformations (Lindenmaier et al., 2017) and comparison with measured infrared intensities for linear alkanes (Williams et al., 2013). The different errors and their trends for the intensities of C–H stretching and HCH bending modes indicate that a simple scaling approach, so successful for frequencies, will not work for intensities. In this work, we have included all conformers within 2 kcal mol−1 of the lowest energy conformer. This limit accounts for > 98 % of the population distribution at 298 K, in most cases. For each HCFC, a relaxed scan was performed to detect all possible conformations. For the C2 compounds, three staggered conformations were examined by rotating the C–C torsional angle by 120. For the C3 compounds, nine possible conformations were calculated by rotating the two torsional angles by 120. Each stable conformer was then fully optimized at the B3LYP/6-31G(2df,p) level followed by a frequency calculation. Conformer populations were calculated for a 298 K Boltzmann's distribution using the relative energies (including a zero-point correction) from the calculations. Including stable conformers resulted in overlapping vibrational bands and, therefore, more congested spectra which is consistent with the observed spectra for HCFCs. A number of the HCFCs have stereoisomers. Although the stereoisomers have identical infrared absorption spectra, they were accounted for in the population distribution. Note that for a molecule with a single asymmetrical carbon (a molecule containing a carbon with four different groups attached), e.g., HCFC-121a (CHClFCCl3), a pair of stereoisomers exist for each conformation and, therefore, the contribution of stereoisomers to the total population factors out. The entire dataset contains 126 molecules with a single asymmetric carbon and 32 molecules containing 2 asymmetric carbons.

A comparison of the experimental and calculated infrared spectrum of HCFC-124a (CHF2CClF2) shown in Fig. 3 demonstrates the importance of including conformers in the spectrum calculation. A comparison of experimental and theoretical spectra for all molecules with experimental data is provided in the Supplement. The calculations found that HCFC-124a has three stable conformers at 298 K with the lowest energy conformer having  50 % of the population. The experimental spectrum is characterized by strong absorption features between 1100 and 1500 cm−1, which are mostly associated with C–F bond vibrations, and C–Cl vibrational modes below 1000 cm−1. The comparison with the experimental spectrum shows that the prominent absorption features at  825, 1000, and 1250 cm−1 originate from the higher energy conformers. The calculated spectrum is in good agreement with the experimentally measured spectrum with band positions and total integrated band strengths agreeing to within  2 %. Note that conformer contributions to an infrared absorption spectrum will be different for different molecules. The impact of including conformers in the radiative efficiency calculations is presented later.

Figure 3Comparison of experimental and calculated infrared absorption spectrum of HCFC-124a (CHF2CClF2). Calculated spectra at B3LYP/6-31G(2df,p) level of theory with (solid red lines) and without (dotted red lines) including stable conformers, and the experimentally measured spectrum (solid black lines) (see Table 1 for the source of the experimental spectrum).

Overall, the agreement between experimental and calculated frequencies was good. Figure S2 shows a comparison of experimental vibrational frequencies with the calculated values. There was a systematic overestimation of the calculated vibrational frequencies above 1000 cm−1 and an underestimation below 1000 cm−1. An empirical frequency correction, which accounts, in part, for anharmonicity and other approximations used in the level of theory employed, was derived from this correlation and applied to all the calculated spectra: νcorrected = 53.609 + 0.94429 ×νcalculated. Using this correction, frequencies around  1200 cm−1 (C–F bond vibrations) and around 800 cm−1 (C–Cl bond vibrations) are shifted by only  1 %. The uncertainty associated with the calculated band positions is estimated to be  1 %. The frequency-corrected spectra were used to derive the metrics reported here.

Figure 4 shows a comparison of calculated and experimental band strengths (integrated between 500 and 2000 cm−1) for the training dataset. Overall, the agreement is good for the majority of HCFCs with the calculated band strengths being within 20 %, or better, of the experimental values. The calculated band strengths are, however, systematically biased high by  20 %, for band strengths < 1.1 × 10−16 cm2 molecule−1 cm−1. A comparison of the training dataset experimental and calculated infrared spectra reveals that the bias originates from a band strength overestimation of bands below 1000 cm−1 that are primarily associated with C–Cl bonds. The bias is greatest for molecules containing more than one Cl atom on the same carbon, e.g., CHFCl2 (HCFC-21), CH3CCl2F (HCFC-141b), and CH2FCCl2F (HCFC-132c). In fact the intensities of C–Cl stretches are a long-known problem for calculation (Halls and Schlegel, 1998). Scaling the overall spectrum strength to account for such biases has been applied to decrease the deviation between experimental and theoretical values in an earlier theoretical study by Betowski et al. (2015). However, since the bias is primarily for the bands associated with C–Cl bonds, a scaling of the entire band strength would not be appropriate nor an accurate representation of the experimental spectrum. The spectra reported here do not include a band strength correction, as the prediction of which bands are overestimated is too uncertain without knowledge of the experimental spectrum. Although it is difficult to estimate the uncertainty for the theoretical calculations, an estimated  20 % band strength uncertainty includes nearly all the training dataset values and encompasses the possible systematic bias observed for certain vibrational bands.

Figure 4Comparison of experimental and calculated infrared band strengths over the 500–2000 cm−1 region for the HCFC training dataset (see Table 1 for the source of the experimental spectra). The dashed line is the 1:1 correlation. The shaded region represents a 20 % spread around the 1:1 line.

Figure 5Sensitivity of the calculated HCFC radiative efficiencies in this study to (a) the inclusion of higher energy conformers and (b) to the broadening of the calculated infrared absorption bands, as described in the text. ΔRE values are relative to the full analysis that includes broadened spectra and all conformers within 2 kcal mole−1 of lowest energy conformer.

As illustrated earlier for HCFC-124a, Fig. 3, stable HCFC conformers can make a significant contribution to its infrared absorption spectrum. Figure 5 shows the impact of including the conformer population on the calculated RE for each of the HCFCs included in this study. Overall, including conformers increases or decreases the calculated RE by 10 %, or less, in most cases. However, there are some HCFCs where a difference of 20 %, or more, is observed, e.g., HCFC-124a, HCFC-151, and HCFC-232ba. In conclusion, including the contribution from populated conformers improves the accuracy of the calculated RE values and decreases potential systematic errors in the theoretically predicted RE values.

The strongest HCFC vibrational bands are due to C–F stretches, 1000–1200 cm−1, which strongly overlap the ”atmospheric window” region. The molecular geometry of the HCFC determines the exact vibrational band frequencies, i.e., HCFCs and their isomers have unique infrared absorption spectra and REs. Note that the calculated infrared spectra in this work include vibrational bands below 500 cm−1, which is usually the lower limit for experimental infrared absorption spectra measurements. The contribution of vibrational bands in this region to the RE is quantified in our calculations and is usually minor, i.e., < 1 %. The Earth's irradiance profile, HCFC infrared absorption spectra, and HCFC radiative efficiency spectra for each HCFC included in this study are included in the Supplement.

Lifetime-adjusted REs were calculated using the CFC-11 emission scenario ”S” shaped parameterization given in Hodnebrog et al. (2013), which is intended to account for non-uniform mixing of the HCFC in the atmosphere. The adjustment is greatest for short-lived molecules. A +10 % correction was applied to all molecules to account for the stratospheric temperature correction (see IPCC, 2013; Supplement Sect. 8.SM.13.4 for the origin of this factor). Well-mixed and lifetime-adjusted RE values are included in the Supplement.

## 2.5 Global warming and global temperature change potentials

Global warming potentials on the 20- and 100-year time horizons (T) were calculated relative to CO2 using the formulation given in IPCC (2013):

$\mathrm{GWP}\left(T\right)=\frac{\mathrm{RE}\mathit{\tau }\left[\mathrm{1}-\mathrm{exp}\left(-T/\mathit{\tau }\right)\right]}{{M}_{\mathrm{HCFC}}\mathrm{Int}\phantom{\rule{0.25em}{0ex}}{\mathrm{RF}}_{{\mathrm{CO}}_{\mathrm{2}}}\left(T\right)},$

where IntRF${}_{{\text{CO}}_{\mathrm{2}}}$(T) is the integrated radiative forcing of CO2 and MHCFC is the HCFC molecular weight. The RE used in the calculation was lifetime-adjusted with a stratospheric temperature correction applied. The global lifetimes were estimated as described in Sect. 2.1. The CO2 denominator is consistent with the GWP values reported in the WMO (2014) and IPCC (2013) assessments corresponding to a CO2 abundance of 391 ppm. Therefore, the values reported in this work can be compared directly to values reported in the WMO and IPCC assessments. A comparison of our training dataset values is given in Fig. 6, where the majority of the GWPs agree to within 15 %. HCFCs-21, -22, -122, and -123 have larger differences, due primarily to discrepancies between the estimated OH rate coefficients and those from the literature. Our GWP results can be scaled to the 2016 CO2 abundance of 403 ppm (NOAA, 2017) by multiplying by 1.03, which accounts for a decrease in the CO2 radiative efficiency (see Myhre et al., 1998; Joos et al., 2013).

Figure 6Comparison of 100-year time horizon GWP values reported in the WMO assessment (WMO, 2014) and McGillen et al. (2015) for 133a (with lifetime-adjustment and stratospheric temperature correction applied) and the values calculated in this study. The dashed line represents the 1:1 correlation and the shaded area is a 15 % spread around the 1:1 line.

Global temperature change potentials were calculated for the 20-, 50-, and 100-year time horizons using the parameterizations given in the IPCC (2013) Supplement Sect. 8.SM.11.2.

3 Results and discussion

Figure 7 provides a comprehensive graphical summary of the lifetime, ODP, lifetime and stratospheric temperature adjusted RE, GWP, and GTP results obtained in this study and the values that are based on experimental data (in black) where available. The metric values for the individual compounds are available in Table S2 and the individual data sheets in the Supplement. A detailed summary of the theoretical results is also included in the data sheets for the individual compounds.

It is clear that the metrics for the C1–C3 HCFCs possess a significant range of values with a dependence on the H-atom content as well as the isomeric form for a given chemical formula. In general, an increase in the HCFC H-atom content leads to a shorter atmospheric lifetime, e.g., the lifetimes for the HCFC-226 compounds (1 H-atom) are greater than most other HCFCs. However, the HCFC reactivity also depends on the distribution of hydrogen, chlorine, and fluorine within the molecule, i.e., the isomeric form and lifetimes for isomers can vary significantly. For example, the lifetime of HCFC-225ca (CHCl2CF2CF3) is 1.9 years, while that of HCFC-225da (CClF2CHClCF3) is 16.3 years. The highest reactivity HCFCs are short-lived compounds with lifetimes as low as  0.3 years. The lowest reactivity HCFCs have lifetimes as long as 60 years (HCFC-235fa, CClF2CH2CF3).

The trends in the HCFC ODPs follow that of the lifetimes with an additional factor to account for the chlorine content of the HCFC. Overall many of the HCFCs have significant ODPs with 33 HCFCs having values greater than 0.1 and 78 greater than 0.05.

In addition to HCFC isomers having different reactivity (lifetimes), each isomer also has a unique infrared absorption spectrum and, thus, a unique RE. The HCFC REs range from a low of  0.03 to a high of  0.35 W m−2 ppb−1. The HCFCs with the highest H-atom content have lower REs, in general, although there are exceptions as shown in Fig. 6. As expected, many of the HCFCs are potent greenhouse gases. The GWPs and GTPs also show a strong isomer dependence, e.g., the GWPs on the 100-year time horizon for the 9 HCFC-225 isomers differ by a factor of  12. The lowest HCFC GWPs in this study are  10 and the greatest value is  5400 for HCFC-235fa.

Figure 7Summary of the results obtained in this study for C1–C3 HCFCs (red and blue) and the values for which experimentally derived metrics are available (black). The lifetime, GWP, and GTP values for HCFC-235fa (CClF2CH2CF3) (gold) have been multiplied by 0.4 to improve the overall graphical clarity.

## Metric uncertainty

The training calculations have been used to estimate the uncertainties in our atmospheric lifetime estimates and infrared absorption spectra and how these uncertainties propagate through to the key ODP, RE, GWP, and GTP metrics. It is not possible to assign a single uncertainty for all HCFCs for each metric due to their dependence on the individual properties of the HCFCs. To provide a general perspective for the reliability of the metrics reported in this study, we limit our discussion to the average behavior.

The predominant atmospheric loss process for HCFCs was shown to be reaction with the OH radical, while UV photolysis in the stratosphere was found to be a non-negligible loss process for HCFCs with long lifetimes and significant Cl content. The DeMore (1996) SAR predicts the training dataset OH rate coefficients at 298 K to within 25 % on average, which directly translates to a 25 % uncertainty in the HCFC tropospheric lifetime. A conservative uncertainty estimate in the predicted OH rate coefficients at 272 K would be  50 %, see Fig. 1. Including an estimated  40 % uncertainty for the stratospheric UV photolysis and O(1D) reactive loss processes increases the global lifetime uncertainty by only  2 %.

Table 2The Annex C HCFC table provided in the Kigali Amendment to the Montreal Protocol, where the range of 100-year time horizon global warming potentials (GWPs) obtained in this work for various HCFC isomers all with the chemical formula listed in the first column is given in italicsa.

a Typos for HCFC 123 and 124 GWPs entries are corrected here. b Identifies the most commercially viable substances. c The ODPs listed are from the Montreal Protocol, while ODPs derived in this work for the individual HCFCs are available in the Supplement, Table S2. d Range of values from this work obtained for the HCFC isomers are given in italics.

The semi-empirical ODP uncertainty is directly proportional to the global lifetime uncertainty with an additional factor to account for the uncertainty in the fractional release factor (FRF). For HCFCs with total lifetimes less than 2 years, the total ODP uncertainty is estimated to be 35 %, for a 25 % uncertainty in the global lifetime. For longer lived HCFCs, the ODP uncertainty is greater, 50 % or more.

The overall uncertainty in the GWP and GTP metrics depends on the lifetime and RE uncertainties, with a different dependence on different time horizons. Compounds with lifetimes of less than 1 year have propagated uncertainties of  55 % on average. As the lifetime increases the uncertainty decreases to  30 % on average, or less. The greater uncertainty values for the shorter lived HCFCs is primarily associated with the uncertainty introduced by the lifetime-adjusted RE.

As mentioned earlier, there have been a number of previous studies that have applied methods similar to those used in the present study. The most relevant of these studies is that of Betowski et al. (2015) who reported radiative efficiencies for a large number of the C1–C3 HCFCs included in this study. Although they report REs for 178 of the 274 HCFCs included in our work there are significant differences between their REs and those reported here. Figure S4 shows a comparison of the RE values calculated here with those reported in Betowski et al. (2015) for the HCFCs common to both studies. The RE values from Betowski et al. (2015) are systematically lower than the ones reported here by  29 % on average. A similar systematic underestimation is observed when the Betowski et al. (2015) RE values are compared with the available HCFC experimental data used in our training dataset. Betowski et al. (2015) used B3LYP/6-31G(d) to calculate the HCFC infrared spectra and applied a band strength correction in their RE calculation. Note that a band strength correction was not applied in the present study as discussed earlier. In addition, Betowski et al. (2015) did not use broadened infrared spectra in their RE calculation and included only the lowest energy conformer. These differences can account for some of the scatter in the correlation shown in Fig. S4. The average difference between the reported RE values can only partially be explained by the different methods used here, B3LYP/6-31G(2df,p), and in Betowski et al. (2015), B3LYP/6-31G(d), as they produce very similar HCFC infrared spectra, i.e., the band strengths obtained with these methods agree to within  10 %.

Betwoski et al. (2015) used the available HCFC experimental data and data for a large number of compounds from other chemical classes in their training dataset, e.g., perhalocarbons, haloaldehydes, haloketones, and haloalcohols. On the basis of their analysis, a band strength scaling factor of 0.699, for the B3LYP/6-31G(d) method, was derived. However, for the HCFCs this scale factor introduces a systematic error in the band strength analysis. In Fig. 4 we showed that the DFT theoretical methods, without scaling, agree with the available experimental HCFC data to within 20 %, or better. Although the HCFC training dataset is relatively small, the band strength scaling factor based on results for other chemical compound classes is most likely not appropriate and introduces a systematic bias for the calculated RE values. Therefore, the infrared spectra reported in the present work and used to derive REs and GWPs were not scaled.

4 Summary

In this study, policy-relevant metrics have been provided for C1–C3 HCFC compounds, many of which were not available at the time of the adoption of the Kigali Amendment. Table 2 summarizes the results from this study in the condensed format used in Annex C of the amended protocol where the range of metrics are reported for each HCFC chemical formula. Metrics for the individual HCFCs are given in Table S2 and the data sheets for each of the HCFCs that contain the explicit kinetic parameters and theoretical results obtained in this work.

We have shown that HCFC isomers have significantly different lifetimes, ODPs, and radiative metrics. Of particular interest are the HCFCs with current significant production and emissions to the atmosphere. Of all the HCFCs listed in Annex C of the amended protocol, HCFCs-121(2), -122(3), -133(3), -141(3), -142(3), and -225(9) are of primary interest (the values in parenthesis are the number of isomers for that chemical formula). Of these 23 compounds, experimentally based metrics are included in the Kigali Amendment for only HCFCs-141b, -142b, -225ca, and -225cb. Therefore, the present work provides policy-relevant information for the other HCFCs.

Although this work has provided a comprehensive set of estimated metrics for the C1–C3 HCFCs that presently do not have experimental data, careful direct fundamental laboratory studies of an intended HCFC would better define the critical atmospheric loss processes (reaction and UV photolysis) used to evaluate atmospheric lifetimes. Laboratory measurements of infrared spectra would also provide specific quantitative results to be used in the determination of the RE, GWP, and GTP metrics. It is anticipated that laboratory measurements could yield uncertainties in the reactive and photolysis loss processes of  10 % and the infrared spectrum of  5 %, or better, which are significantly less than the 25 and 20 % average estimated uncertainties obtained with the methods used in this work. Therefore, laboratory studies would potentially yield more accurate metrics. Note that the absolute uncertainty in the ODP, RE, GWP, and GTP metrics would also include a consideration of the uncertainties associated with lifetime determination methods and the Earth's irradiance profile approximation used to derive RE values, as well as the uncertainty in CO2 radiative forcing, which were not considered in this work.

Data availability
Data availability.

Figures and tables including the master summary table of metrics for all HCFCs are provided in the supporting material. Data sheets for the individual HCFCs that contain the derived atmospheric lifetimes, ODP, RE, GWP, and GTP metrics, graphs, figures, and tables of the theoretical calculation results are available at https://www.esrl.noaa.gov/csd/groups/csd5/datasets/.

Supplement
Supplement.

Competing interests
Competing interests.

The authors declare that they have no conflict of interest.

Acknowledgements
Acknowledgements.

This work was supported in part by NOAA Climate Program Office Atmospheric Chemistry, Carbon Cycle, and Climate Program and NASA's Atmospheric Composition Program. The authors acknowledge helpful discussion with Sophia Mylona of the United Nations Environment Programme and David Fahey. The authors acknowledge the NOAA Research and Development High Performance Computing Program (http://rdhpcs.noaa.gov) and the University of North Texas chemistry cluster purchased with support from the NSF Grant CHE-1531468 for providing computing and storage resources that contributed to the research results reported within this paper.

Edited by: Andreas Engel
Reviewed by: three anonymous referees

References

Alecu, I. M., Zheng, J., Zhao, Y., and Truhlar, D. G.: Computational thermochemistry: Scale factor databases and scale factors for vibrational frequencies obtained from electronic model chemistries, J. Chem. Theory Comput., 6, 2872–2887, https://doi.org/10.1021/ct100326h, 2010.

Baasandorj, M., Fleming, E. L., Jackman, C. H., and Burkholder, J. B.: O(1D) kinetic study of key ozone depleting substances and greenhouse gases, J. Phys. Chem. A, 117, 2434–2445, https://doi.org/10.1021/jp312781c, 2013.

Barone, V.: Anharmonic vibrational properties by a fully automated second-order perturbative approach, J. Chem. Phys., 122, 014108, https://doi.org/10.1063/1.1824881, 2005.

Bernard, F., Papanastasiou, D. K., Papadimitriou, V. C., and Burkholder, J. B.: Infrared absorption spectra of linear (L2-L5) and cyclic (D3-D6) permethylsiloxanes, J. Quant. Spect. Rad. Transf., 202, 247–254, https://doi.org/10.1016/j.jqsrt.2017.08.006, 2017.

Betowski, D., Bevington, C., and Allison, T. C.: Estimation of radiative efficiency of chemicals with potentially significant global warming potential, Environ. Sci. Technol., 50, 790–797, https://doi.org/10.1021/acs.est.5b04154, 2015.

Blowers, P. and Hollingshead, K.: Estimations of global warming potentials from computational chemistry calculations for CH2F2 and other fluorinated methyl species verified by comparison to experiment, J. Phys. Chem. A, 113, 5942–5950, https://doi.org/10.1021/jp8114918, 2009.

Bravo, I., Aranda, A., Hurley, M. D., Marston, G., Nutt, D. R., Shine, K. P., Smith, K., and Wallington, T. J.: Infrared absorption spectra, radiative efficiencies, and global warming potentials of perfluorocarbons: comparison between experiment and theory, J. Geophys. Res., 115, D24317, https://doi.org/10.1029/2010JD014771, 2010.

Burkholder, J. B., Sander, S. P., Abbatt, J., Barker, J. R., Huie, R. E., Kolb, C. E., Kurylo, M. J., Orkin, V. L., Wilmouth, D. M., and Wine, P. H.: “Chemical Kinetics and Photochemical Data for Use in Atmospheric Studies, Evaluation No. 18”, JPL Publication 15–10, Jet Propulsion Laboratory, Pasadena, 2015, available at: http://jpldataeval.jpl.nasa.gov, 2015.

Carnimeo, I., Puzzarini, C., Tasinato, N., Stoppa, P., Pietropolli Charmet, A., Biczysko, M., Cappelli, C., and Barone, V.: Anharmonic theoretical simulations of infrared spectra of halogenated organic compounds, J. Chem. Phys., 139, 074310, https://doi.org/10.1063/1.4817401, 2013.

Charmet, P. A., Stoppa, P., Tasinato, N., Giorgianni, S., Barone, V., Biczysko, M., Bloino, J., Cappelli, C., Carnimeo, I., and Puzzarini, C.: An integrated experimental and quantum-chemical investigation on the vibrational spectra of chlorofluoromethane, J. Chem. Phys., 139, 164302, https://doi.org/10.1063/1.4825380, 2013.

DeMore, W. B.: Experimental and Estimated Rate Constants for the Reactions of Hydroxyl Radicals with Several Halocarbons, J. Phys. Chem., 100, 5813–5820, https://doi.org/10.1021/jp953216+, 1996.

Engel, A., Bönisch, H., Ostermöller, J., Chipperfield, M., Dhomse, S., and Jöckel, P.: A refined method for calculating equivalent effective stratospheric chlorine, Atmos. Chem. Phys., 18, 601–619, https://doi.org/10.5194/acp-18-601-2018, 2018.

Etminan, M., Highwood, E. J., Laube, J. C., McPheat, R., Marston, G., Shine, K. P., and Smith, K. M.: Infrared absorption spectra, radiative efficiencies, and global warming potentials of newly-detected halogenated compounds: CFC-113a, CFC-112 and HCFC-133a, Atmosphere, 5, 473–483, https://doi.org/10.3390/atmos5030473, 2014.

Frisch, M. J., Trucks, G. W., Schlegel, H. B., Scuseria, G. E., Robb, M. A., Cheeseman, J. R., Scalmani, G., Barone, V., Petersson, G. A., Nakatsuji, H., Li, X., Caricato, M., Marenich, A., Janesko, J. B. B. G., Gomperts, R., Mennucci, B., Hratchian, H. P., Ortiz, J. V., Izmaylov, A. F., Sonnenberg, J. L., Williams-Young, D., Ding, F., Lipparini, F., Egidi, F., Goings, J., Peng, B., Henderson, A. P. T., Ranasinghe, D., Zakrzewski, V. G., Gao, J., Rega, N., Zheng, G., Liang, W., Hada, M., Ehara, M., Toyota, K., Fukuda, R., Hasegawa, J., Ishida, M., Nakajima, T., Honda, Y., Nakai, O. K. H., Vreven, T., Throssell, K. J. A., Montgomery, J., Peralta, J. E., Ogliaro, F., Bearpark, M., Heyd, J. J., Brothers, E., Kudin, K. N., Staroverov, V. N., Keith, T., Kobayashi, R., Raghavachari, J. N. K., Rendell, A., Burant, J. C., Iyengar, S. S., Tomasi, J., Cossi, M., Millam, J. M., Klene, M., Adamo, C., Cammi, R., Ochterski, J. W., Martin, R. L., Morokuma, K., Farkas, O., Foresman, J. B., and Fox, D. J.: Gaussian 09, Revision A.02, Gaussian, Inc., Wallingford CT, 2016.

Halls, M. D. and Schlegel, H. B.: Comparison of the performance of local, gradient-corrected, and hybrid density functional models in predicting infrared intensities, J. Chem. Phys., 109, 10587–10593, doi;10.1063/1.476518, 1998.

Hodnebrog, Ø., Etminan, M., Fuglestvedt, J. S., Marston, G., Myhre, G., Nielsen, C. J., Shine, K. P., and Wallington, T. J.: Global warming potentials and radiative efficiencies of halocarbons and related compounds: A comprehensive review, Rev. Geophys., 51, 300–378, https://doi.org/10.1002/rog.20013, 2013.

Hout, R. F., Levi, B. A., and Hehre, W. J.: Effect of electron correlation on theoretical vibrational frequencies, J. Comput. Chem., 3, 234–250, https://doi.org/10.1002/jcc.540030216, 1982.

IPCC: Climate Change 2013: The Physical Science Basis, Contribution of Working Group 1 to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change, edited by: Stocker, T. F., Qin, D., Plattner, G.-K., Tignor, M., Allen, S. K., Boschung, J., Nauels, A., Zia, Y., Bex, V., and Midgley, P. M., Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA., 2013.

Jiménez-Hoyos, C. A., Janesko, B. G., and Scuseria, G. E.: Evaluation of range-separated hybrid density functionals for the prediction of vibrational frequencies, infrared intensities, and Raman activities, Phys. Chem. Chem. Phys., 10, 6621–6629, https://doi.org/10.1039/b810877c, 2008.

Joos, F., Roth, R., Fuglestvedt, J. S., Peters, G. P., Enting, I. G., von Bloh, W., Brovkin, V., Burke, E. J., Eby, M., Edwards, N. R., Friedrich, T., Frölicher, T. L., Halloran, P. R., Holden, P. B., Jones, C., Kleinen, T., Mackenzie, F. T., Matsumoto, K., Meinshausen, M., Plattner, G.-K., Reisinger, A., Segschneider, J., Shaffer, G., Steinacher, M., Strassmann, K., Tanaka, K., Timmermann, A., and Weaver, A. J.: Carbon dioxide and climate impulse response functions for the computation of greenhouse gas metrics: a multi-model analysis, Atmos. Chem. Phys., 13, 2793–2825, https://doi.org/10.5194/acp-13-2793-2013, 2013.

Katsyuba, S. A., Zvereva, E. E., and Burganov, T. I.: Is there a simple way to reliable simulations of infrared spectra of organic compounds?, J. Phys. Chem. A, 117, 6664–6670, https://doi.org/10.1021/jp404574m, 2013.

Kazakov, A., McLinden, M. O., and Frenkel, M.: Computational design of new refrigerant fluids based on environmental, safety, and thermodynamic characteristics, Ind. Chem. Eng. Res., 51, 12537–12548, https://doi.org/10.1021/ie3016126, 2012.

Kigali Amendment to the Montreal Protocol on Substances that Deplete the Ozone Layer, available at: http://ozone.unep.org/en/handbook-montreal-protocol-substances-deplete-ozone-layer/41453, 2016.

Ko, M. K. W., Newman, P. A., Reimann, S., Strahan, S. E., Plumb, R. A., Stolarski, R. S., Burkholder, J. B., Mellouki, W., Engel, A., Atlas, E. L., Chipperfield, M., and Liang, Q.: Lifetimes of stratospheric ozone-depleting substances, their replacements, and related species, available at: http://www.sparc-climate.org/publications/sparc-reports/sparc-report-no-6/ (last access: May 2018) 2013.

Kwok, E. S. C. and Atkinson, R.: Estimation of hydroxyl radical reaction rate constants for gas-phase organic compounds using a structure-reactivity relationship: An update, Atmos. Environ., 29, 1685–1695, 1995.

Leedham Elvidge, E., Bönisch, H., Brenninkmeijer, C. A. M., Engel, A., Fraser, P. J., Gallacher, E., Langenfelds, R., Mühle, J., Oram, D. E., Ray, E. A., Ridley, A. R., Röckmann, T., Sturges, W. T., Weiss, R. F., and Laube, J. C.: Evaluation of stratospheric age of air from CF4, C2F6, C3F8, CHF3, HFC-125, HFC-227ea and SF6; implications for the calculations of halocarbon lifetimes, fractional release factors and ozone depletion potentials, Atmos. Chem. Phys., 18, 3369–3385, https://doi.org/10.5194/acp-18-3369-2018, 2018.

Lindenmaier, R., Williams, S. D., Sams, R. L., and Johnson, T. J.: Quantitative infrared absorption spectra and vibrational assignments of crotonaldehyde and methyl vinyl ketone using gas-phase mid-infrared, far-infrared, and liquid raman spectra: s-cis vs s-trans composition confirmed via temperature studies and ab initio methods, J. Phys. Chem. A, 121, 1195–1212, https://doi.org/10.1021/acs.jpca.6b10872, 2017.

McGillen, M. R., Bernard, F., Fleming, E. L., and Burkholder, J. B.: HCFC-133a (CF3CH2Cl): OH rate coefficient, UV and infrared absorption spectra, and atmospheric implications, Geophys. Res. Lett., 42, 6098–6105, https://doi.org/10.1002/2015GL064939, 2015.

Montreal Protocol on Substances that Deplete the Ozone Layer (1987), available at: http://unep.ch/ozone/pdf/Montreal-Protocol2000.pdf (last access: May 2018), 1987.

Myhre, G., Highwood, E. J., Shine, K. P., and Stordal, F.: New estimates of radiative forcing due to well mixed greenhouse gases, Geophys. Res. Lett., 25, 2715–2718, https://doi.org/10.1029/98GL01908, 1998.

National Institute of Standards and Technology (NIST), Computational Chemistry Comparison and Benchmark Database, NIST Standard Reference Database Number 101, Release 18, October 2016, edited by: Johnson, Russell D. III, available at: http://cccbdb.nist.gov/ (last access: April 2018), 2016.

National Oceanic and Atmospheric Administration (NOAA), Earth System Research Laboratory, Global Monitoring Division, Global Greenhouse Gas Reference Network, available at: https://www.esrl.noaa.gov/gmd/ccgg/trends/global.html (last access: April 2018), 2017.

NOAA, Earth System Research Laboratory, Chemical Sciences Division, available at: https://www.esrl.noaa.gov/csd/groups/csd5/datasets/ (last access: May 2018), 2018

Orkin, V. L., Guschin, A. G., Larin, I. K., Huie, R. E., and Kurylo, M. J.: Measurements of the infrared absorption cross-sections of haloalkanes and their use in a simplified calculational approach for estimating direct global warming potentials, J. Photochem. Photobiol. A-Chem., 157, 211–222, 2003.

Ostermöller, J., Bönisch, H., Jöckel, P., and Engel, A.: A new time-independent formulation of fractional release, Atmos. Chem. Phys., 17, 3785–3797, https://doi.org/10.5194/acp-17-3785-2017, 2017a.

Ostermöller, J., Bönisch, H., Jöckel, P., and Engel, A.: Corrigendum to “A new time-independent formulation of fractional release” published in Atmos. Chem. Phys., 17, 3785–3797, Atmos. Chem. Phys., 17, 3785–3797, https://doi.org/10.5194/acp-17-3785-2017-corrigendum, 2017b.

Papadimitriou, V. C. and Burkholder, J. B.: OH radical reaction rate coefficients, infrared spectrum, and global warming potential of (CF3)2CFCH=CHF (HFO-1438ezy(E)), J. Phys. Chem. A, 120, 6618–6628, https://doi.org/10.1021/acs.jpca.6b06096, 2016.

Papadimitriou, V. C., Portmann, R. W., Fahey, D. W., Mühle, J., Weiss, R. F., and Burkholder, J. B.: Experimental and theoretical study of the atmospheric chemistry and global warming potential of SO2F2, J. Phys. Chem. A, 112, 12657–12666, https://doi.org/10.1021/jp806368u, 2008a.

Papadimitriou, V. C., Talukdar, R. K., Portmann, R. W., Ravishankara, A. R., and Burkholder, J. B.: CF3CF=CH2 and (Z)-CF3CF=CHF: temperature dependent OH rate coefficients and global warming potentials, Phys. Chem. Chem. Phys., 10, 808–820, https://doi.org/10.1039/b714382f, 2008b.

Pople, J. A., Schlegel, H. B., Krishnan, R., Defrees, D. J., Binkley, J. S., Frisch, M. J., Whiteside, R. A., Hout, R. F., and Hehre, W. J.: Molecular orbital studies of vibrational frequencies, Int. J. Quantum Chem., 20, 269–278, https://doi.org/10.1002/qua.560200829, 1981.

Scott, A. P. and Radom, L.: Harmonic vibrational frequencies: An evaluation of Hartree-Fock, Møller-Plesset, quadratic configuration interaction, density functional theory, and semiempirical scale factors, J. Phys. Chem., 100, 16502–16513, https://doi.org/10.1021/jp960976r, 1996.

Sharpe, S. W., Johnson, T. J., Sams, R. L., Chu, P. M., Rhoderick, G. C., and Johnson, P. A.: Gas-phase databases for quantitative infrared spectroscopy, Appl. Spect., 58, 1452–1461, 2004.

Sihra, K., Hurley, M. D., Shine, K. P., and Wallington, T. J.: Updated radiative forcing estimates of 65 halocarbons and nonmethane hydrocarbons, J. Geophys. Res., 106, 20493–20505, 2001.

Solomon, S. and Albritton, D. L.: Time-dependent ozone depletion potentials for short- and long-term forecasts, Nature, 357, 33–37, https://doi.org/10.1038/357033a0, 1992.

UN Environment OzonAction Fact Sheet, available at: http://www.unep.fr/ozonaction/information/mmcfiles/7809-e-factsheet_Kigali_Amendment_to_MP_2017.pdf, 2017.

Wallington, T. J., Pivesso, B. P., Lira, A. M., Anderson, J. E., Nielsen, C. J., Andersen, N. H., and Hodnebrog, Ø.: CH3Cl, CH2Cl2, CHCl3, and CCl4: Infrared spectra, radiative efficiencies, and global warming potentials, J. Quant. Spec. Rad. Trans., 174, 56–64, https://doi.org/10.1016/j.jqsrt.2016.01.029, 2016.

Williams, S. D., Johnson, T. J., Sharpe, S. W., Yavelak, V., Oates, R. P., and Brauer, C. S.: Quantitative vapor-phase IR intensities and DFT computations to predict absolute IR spectra based on molecular structure: I. Alkanes, J. Quant. Spectrosc. Radiat. Trans., 129, 298–307, https://doi.org/10.1016/j.jqsrt.2013.07.005, 2013.

World Meteorological Organization (WMO), Scientific Assessment of Ozone Depletion: 2014, Global Ozone Research and Monitoring Project-Report No. 55 416, Geneva, Switzerland, 2014.