Long-duration observations of Neptune’s brightness at two visible wavelengths provide a disk-averaged estimate of its atmospheric aerosol. Brightness variations were previously associated with the 11-year solar cycle, through solar-modulated mechanisms linked with either ultraviolet or galactic cosmic ray (GCR) effects on atmospheric particles. Here, we use a recently extended brightness data set (1972–2014), with physically realistic modelling to show, rather than alternatives, ultraviolet and GCR are likely to be modulating Neptune’s atmosphere in combination. The importance of GCR is further supported by the response of Neptune’s atmosphere to an intermittent 1.5- to 1.9-year periodicity, which occurred preferentially in GCR (not ultraviolet) during the mid-1980s. This periodicity was detected both at Earth, and in GCR measured by Voyager 2, then near Neptune. A similar coincident variability in Neptune’s brightness suggests nucleation onto GCR ions. Both GCR and ultraviolet mechanisms may occur more rapidly than the subsequent atmospheric particle transport.
Long-term observations of Neptune from a ground-based telescope show variations in the planet’s disk-averaged brightness, which are associated with changes in the reflectivity (albedo) of the planet from its atmospheric aerosol and clouds. Although seasonal variations dominate the time series, Lockwood and Thompson1 showed, using data from 1972 to 1996, that small fluctuations in Neptune’s brightness at two visible wavelengths followed the 11-year solar cycle. They examined two quantities known to vary closely with solar activity. The first, solar ultraviolet radiation, is linked to photochemical variations in Neptune’s atmospheric aerosol particles, and the second, galactic cosmic rays (GCR), may create some of Neptune’s aerosol through ion-induced nucleation. It was not possible to discriminate between the ultraviolet and GCR effects, although the relationship with ultraviolet was slightly more statistically robust1. The Neptune magnitude-solar activity relationship broke down after 1996 (refs 1, 2), but recent extension of the data3 encourages its re-examination. Supporting evidence for a solar cycle in infrared observations from 1975 to 2007 (ref. 4) further motivates a fresh consideration of the origin of the short-term variability in Neptune’s albedo.
Both the ultraviolet and GCR mechanisms can, in principle, account for the changes observed in the photometric observations, which originate in Neptune’s stratosphere and troposphere1,5. The ultraviolet mechanism was originally proposed6 to explain the solar cycle signal when it was first reported in Neptune’s albedo7. It was suggested that ultraviolet-triggered surface chemistry on pre-existing aerosol particles varied the optical properties of Neptune’s stratospheric aerosol through a darkening in colour (‘tanning’), detectable in the photometric measurements. The GCR-driven mechanism was proposed for Neptune8,9, through direct (‘Wilson’) condensation of supersaturated gas onto atmospheric ions10, causing particle growth ultimately detectable at optical wavelengths. The possibility that charge-related effects could modulate the atmospheres of the outer planets, where variations in solar irradiance are proportionately less important11, contrasts with the small likely role of energetic particles in Earth’s atmosphere12 and provides a further motivation for this study.
The two proposed mechanisms for external solar forcing of Neptune are essentially heliospheric (through GCR) or photospheric (through solar ultraviolet) in origin. The analysis to investigate them here uses two approaches. First, the relationships between Neptune’s magnitude, solar ultraviolet radiation and GCRs are studied with multiple regression, allowing both the proposed mechanisms to act together. We find that, when the extra degrees of freedom are accounted for, including both ultraviolet and GCR improves prediction of the magnitude fluctuations. Second, we examine the relatively rapid fluctuations apparent during the mid-1980s in the Neptune astronomical data. This enhanced variability coincided with a known episode of quasi-periodic fluctuations present in GCR13, centred around 1.68 years. Investigating Neptune’s atmospheric variability in the 1.5 to 2 year range therefore presents a method by which to separate the two different suggested solar-modulated influences, an approach previously used to separate coincident terrestrial atmospheric responses14.
The extended Neptune photometric data set 1972–2014
Regular photometric observations of the magnitude (brightness) of Neptune have been made since 1972, through well-characterised visible bandpass filters of width ∼20 nm centred at 472 nm (‘b’, blue) and 551 nm (‘y’, green) using a 21-in telescope at Lowell Observatory, Arizona2, Fig. 1a. Each magnitude value is typically determined from between 4 and 39 nights of data (median 9 nights), taken around the time the planet is brightest in the sky (opposition)3. Standard errors in the magnitude measurements, determined from the standard deviations and number of nights of observation were typically ±0.001 (ref. 3). Sampling intervals varied between 0.7 and 1.2 years, with median interval of 1.04 years. Figure 1 summarizes the data, with Fig. 1a showing the measured magnitudes, Fig 1b showing the magnitude fluctuations, Fig. 1c showing the ultraviolet data and Fig. 1d showing GCR measured both at Earth and in space. More information on the data is given in the ‘Methods’ section.
The correlation between the 29 data points and 30-day running means of ultraviolet, sunspots and GCR with a range of lags was calculated previously1. The correlation between Neptune’s magnitude fluctuations and ultraviolet was statistically significant, whereas the correlation with GCR was not, on which basis it was concluded that ultraviolet was the more likely mechanism1. This analysis1 did not allow for the possibility that both the physically plausible mechanisms involving ultraviolet and GCR could be acting in combination in Neptune’s atmosphere to cause the observed albedo variations. If so, multiple regression may be more appropriate than treating the two proposed mechanisms independently. The earlier analysis1 was statistically rather than physically based, whereas we have used standard ion–aerosol theory to guide our statistical approach. Finally, extra data have recently been made available3, which we now include.
Previous analyses1 assumed linear relationships between ultraviolet (UV) and albedo, and GCR and albedo. Although the ultraviolet-albedo relationship is generally assumed to be linear6, this assumption is not necessarily appropriate for the GCR mechanism. In this case, the albedo changes are likely to be proportional to the number of ion-induced particles. The number of particles formed is controlled by the ion-induced nucleation rate9, which is proportional to the atmospheric ion (or electron) concentration n, where the ions are singly charged, nanometre-sized clusters created by GCR ionization11 with volumetric production rate q. In ion–aerosol theory, there are two possible limiting regimes linking n and q. First, the recombination limit of negligible aerosol, in which the ion concentration n is controlled by ion–ion or ion–electron self-recombination and . Second, in the attachment regime, the ion concentration is limited by attachment to any pre-existing particles (such as aerosols, haze, clouds or dust) and n∝q (for example, see ref. 11). Assuming that the GCR count rate provides an estimate of q (for example, see ref. 15), a set of possible statistical relationships was investigated of the form:
where fb,y are the measured magnitude fluctuations in the b (472 nm) or y (551 nm) wavelength ranges, κ, λ and μ are coefficients for the b or y data representing the ultraviolet mechanism, ion attachment and ion recombination, respectively, and x is a constant for the b or y data. Daily Lyman-alpha and Oulu neutron counter (GCR) data, averaged for ±20 days around the observation date given in ref. 3, were used as measurements of ultraviolet (UV) and GCR (see the ‘Methods’ section). The regressions were weighted according to the standard errors in the magnitude data described above, and the errors in ultraviolet and GCR data were assumed to be negligible in comparison with those in the magnitude data. As the attachment and recombination regimes cannot act simultaneously at the same location, this set of statistical relationships represents the integrated effect of the different atmospheric layers observed at Earth through each filter.
The adjusted coefficient of determination (R2), that is, fraction of the variance explained by the fit, corrected for the number of points and fitted variables, was used to evaluate each model, summarized in Table 1. For the y filter, adjusted R2 was improved to 0.14 (see case 7 in Table 1) when both the ultraviolet and GCR-related mechanisms were included rather than considering the mechanisms separately, which only explained 2–8% of the variance. Considering both GCR-created ionization and ultraviolet therefore permits rejection of the null hypothesis, which is that including both ultraviolet and GCR does not improve the fit (for example, see ref. 16). The improvement from including both GCR and ultraviolet is less marked for the b filter data, with the fit between ultraviolet and magnitude fluctuation slightly better than for GCR, ultraviolet and magnitude fluctuation. The measured and modelled magnitude fluctuations are compared in Fig. 2.
One possible explanation for the differences between the b and y filter responses relates to the different parts of Neptune’s atmosphere accessed by each filter. The 442 nm b filter responds to stratospheric haze particles, whereas the 551 nm y filter is more sensitive to the optical properties of tropospheric aerosols6. Ultraviolet will be absorbed by, for example, haze layers17 as it passes through the atmosphere, whereas highly energetic secondary GCR, typically muons of several GeV, can readily penetrate the deep atmosphere (for example, see ref. 11), with the maximum ionization, known in the terrestrial atmosphere as the Pfotzer–Regener maximum15, expected at about 40 hPa (ref. 9). It is therefore plausible that particles seen by the b filter in the haze layers would respond preferentially to ultraviolet, but that the changes in the y filter wavelength can be better explained by the inclusion of GCR in the model.
Particle detectors on the Voyager 2 spacecraft measured primary GCR as they passed out of the Solar System. These measurements showed variability on 1 to 2 year timescales18, which was at its strongest in primary GCR in the 1980s, consistently with terrestrial neutron monitor data19. Although similar variability is apparent in terrestrial GCR (neutron monitor) measurements, it is not in the solar 10.7-cm radio flux, a widely-used index of solar radiative emissions20. Beyond GCR data, this variability in the 1980s has also been identified in other heliospherically modulated quantities19, such as terrestrial surface atmospheric electricity data21. In contrast, such variability is not apparent in photospheric quantities such as solar ultraviolet, which makes this periodicity a useful diagnostic for separating photospheric and heliospherically modulated effects14.
To pursue this for Neptune’s atmosphere we consider whether the cosmic ray variability observed at Earth is also present at Neptune. After establishing that it is, we then consider when the variability on these timescales occurs in Neptune’s atmosphere, GCR and, for completeness, solar ultraviolet. One approach to evaluating variations such as these within specified frequency ranges is to use a periodogram, or a series of periodograms selecting successive time intervals. Using successive periodograms, calculated using the Lomb–Scargle method for irregularly spaced data, the temporal variations of spectral power density (SPD) between 1.5 and 1.9 years in Neptune’s magnitude, cosmic rays from both Voyager 2 and Oulu and ultraviolet (Lyman-alpha) radiation are shown in Fig. 3 as a moving-window spectrogram. The cosmic ray data used are protons of energy >70 MeV measured by the Voyager 2 Low Energy Charged Particle (LECP) instrument22. Figure 3a presents a spectrogram of the data from Voyager 2, indicating strong spectral power at 1.5–1.9-year periodicities from about 1983 to 1987, when Voyager 2 was travelling from Saturn to Neptune. (Further details of the spectral data processing are given in the ‘Methods’ section). Voyager 2’s closest approach to Uranus was on 24 January 1986, and to Neptune on 25 August 1989 (ref. 23).
Figure 3a–c shows spectrograms generated from the data collected at Neptune, Fig. 3d shows terrestrial cosmic rays measured at Oulu in Finland and Fig. 3e shows the ultraviolet data. The Oulu and Voyager 2 cosmic ray data support earlier findings17, in that the spectral variability appears first in GCR at Earth (Fig. 3d), before reaching Voyager 2 (Fig. 3a) consistent with outward propagation of a heliospheric feature. The Neptune and Voyager 2 spectrograms show similarities in their time evolution, with coincident increased SPD during the 1980s. To evaluate the significance of this enhanced SPD, a Monte-Carlo procedure was used. Using random shuffling of the magnitude fluctuation data, many (50,000) randomised power spectra were obtained; a spectral peak at ∼1.6 years has a probability of being caused by chance of about 1% (P<0.02), see Fig. 4.
In contrast, the spectrogram derived from the Lyman-alpha data (Fig. 3e) shows minimal variability in the range of periodicities considered during the mid-1980s. Hence the Voyager 2 cosmic ray data establish that the 1.5–1.9-year periodicity was present both in Neptune’s atmosphere and in GCR near Neptune during the 1980s.
The 1.5–1.9-year spectral feature in heliospheric GCR can be used as a ‘fingerprint’ of a possible GCR influence in atmospheric properties such as clouds14. Comparing the strength of this feature on Neptune with GCR therefore provides a method to separate ultraviolet and GCR effects on Neptune’s albedo. However, there may be a lag in Neptune’s measured albedo in response to external forcing, due to the internal timescales of particle production and movement in Neptune’s atmosphere. These processes were described6 as methane being injected into the stratosphere and upper troposphere by convection, where photochemical, nucleation and sedimentation processes act on timescales of typically a few Earth years. The photochemical colour changes postulated to be the ultraviolet mechanism providing solar modulation of the albedo are thought to act on 0.2–2-year timescales6. Guided by these ideas, it was found that the fit statistics summarized in Table 1 could be improved by allowing Neptune’s albedo to lag ultraviolet and GCR.
We have further investigated the delays in Neptune’s atmospheric response by carrying out a lag correlation analysis between the average 1.5–1.9-year SPD in GCR, as for Fig. 3, and the same quantity in Neptune’s magnitude, Fig. 5a. The peak response is achieved at a lag of 3 years for both wavelengths, and Fig. 5b indicates that, with a 3-year lag, 32% of the variance in the Neptune 472 nm SPD can be explained by GCR at P<0.001 confidence (18% for the 551 nm SPD at P<0.05 confidence). The calculated lag is robust to errors in the SPD, as determined by recalculating the spectra many (10,000) times, including a normally distributed random error within the quoted uncertainty on the magnitude measurements3. Supplementary Fig. 1 is a version of Fig. 5 calculated for the 1.5–1.9-year SPD in Lyman-alpha (ultraviolet) radiation. Unlike the GCR-magnitude relationship in SPD (Fig. 5) which shows an almost linear dependency in the 1980s, there is no statistically significant linear effect between the 482 nm SPD and ultraviolet (or, indeed, for the 551 nm SPD against the ultraviolet SPD, not plotted). This indicates that some of the spectral features previously identified in the GCR data during the 1980s have propagated into Neptune’s atmosphere for detection at 472 nm, which is not replicated for the ultraviolet data.
Returning to the GCR effects, and restricting the analysis to data from the 1980s, when the spectral feature was particularly strong and known to be present close to Neptune, then 87% of the variance in this intermittent periodicity at 472 nm can be explained solely by GCR at the P<0.001 confidence level. For the y data at 551 nm, the R2 remains 18% during the 1980s.
Estimates using classical cloud physics theory24 for plausible parameters of ion-induced particle growth at Neptune (see the ‘Methods’ section) indicate that newly nucleated particles could grow to optical wavelengths relatively quickly, with timescales from tens of minutes to hours. This rapid ion growth timescale implies that the lagged GCR effects observed in Neptune’s magnitude fluctuations could arise from the propagation of the 1.5–1.9-year periodicity outwards through the heliosphere, suggested by the lag between the spectral features in Voyager 2 (Fig. 3a) and Oulu (Fig. 3d).
The two analyses presented in this paper, by multiple regression and spectral techniques, represent different effects. The multiple regression evaluates the net response of Neptune’s magnitude to both GCR and ultraviolet forcing, whereas the SPD approach only addresses the sensitivity of Neptune’s atmosphere to one forcing, that of GCR on 1.5–1.9-year timescales. For 472 nm, variability at these periodicities during the 1980s is well explained by GCR. In terms of net response over the whole data set (1972–2014), fluctuations in the 472 nm filter data are most effectively accounted for by ultraviolet variations alone, but at 551 nm there is a combined effect of GCR and ultraviolet.
Two alternative origins have previously been proposed2 for the decadal variations observed in Neptune’s atmosphere, external forcing (solar modulation) or chance. On the basis of a statistical argument, GCR or ultraviolet presented alternatives as solar forcing agents1. Including the most recent data, we now find that considering GCR and ultraviolet as joint contributors to Neptune’s atmospheric variability is stronger than an either–or scenario. Our model’s explanatory power is enhanced by including realistic ion–aerosol physics, allowing for ion loss both by attachment to aerosol and by ion–ion or ion–electron recombination.
Ion–aerosol theory considerations indicate that, in cloudy or hazy conditions, ions attach to aerosol particles (see equation 1). This has two consequences. First, haze particles or cloud droplets will become charged by ion attachment. The charge does not depend on the ionization rate25, so will not generate the photometric variability analysed here. Second, the associated ion depletion will reduce opportunities for ion-induced nucleation. As Neptune’s stratosphere and troposphere are rich in haze and cloud particles5,6, this suggests a role for transport processes6,26 in moving nucleated particles to regions where they become detectable in the photometric observations.
Our work provides new evidence for solar forcing in Neptune’s atmosphere on sub-seasonal timescales, through both ultraviolet-driven and GCR mechanisms. The lags in Neptune’s response to external forcing present in both GCR and ultraviolet data over the entire time series, and in the GCR SPD during the 1980s, are consistent both with each other and with known particle movement timescales6. Further investigation is needed to understand the potentially very different timescales associated with both particle-modulating mechanisms, and the relevant transport processes within Neptune’s atmosphere.
Neptune magnitude data
The Neptune magnitude data has been obtained by Dr W Lockwood and collaborators from the Lowell Observatory, Arizona over many years2,3. Neptune’s magnitude is measured with a 21-in reflector telescope using differential photometry, a technique based on measuring the brightness of a target object relative to comparison stars. The data are filtered in the visible with filters called ‘b’ (centred on 472 nm) and ‘y’ (centred on 551 nm). Filter-response functions and details of the long-term stability and errors are all given in ref. 2.
Detrending the Neptune magnitude data is necessary to remove the slow seasonal related increase in Neptune’s brightness (for example, see refs 1, 2, 27). Following the approach in ref. 1, we have applied smoothing curves to the magnitude data to remove the low-frequency seasonal changes and look at fluctuations occurring on more rapid timescales. A quadratic detrend was applied in earlier analyses1,2, but rather than assume an arbitrary polynomial, we have applied robust local smoothing methods and compared them with the quadratic in Fig. 6a. The lowess28 fit and the newer algorithm, loess29, are well-established non-parametric local smoothers, weighted towards points near the region to be fitted. It can be seen from Fig. 6b that the key features in the magnitude fluctuations are preserved independently of the smoothing fit chosen.
A Kolmogorov–Smirnov (KS) statistical test has also been used to establish whether the magnitude fluctuations calculated using any of the three smoothing fits differ statistically. Importantly, the Kolmogorov–Smirnov test does not make any assumptions about the distribution of the data (for example, see ref. 30). Table 2 indicates that for most of the types of smoothing used, the calculated magnitude fluctuations are not significantly different.
Cosmic ray data
GCRs are energetic particles generated outside the Solar System. They are mainly protons, which are most abundant, and alpha particles (helium nuclei)31. Cosmic rays ionize atmospheres by colliding with molecules and inducing a cascade of secondary ionizing and non-ionizing particles; they are the major source of ionization in many planetary atmospheres11. Neutron monitor measurements of GCR are used here as an indicator of atmospheric ionization. Neutrons are non-ionizing radiation formed by GCR decaying in Earth’s atmosphere and are measured by a network of terrestrial monitors, described below. GCR can also be measured directly by spacecraft. Voyager 2 proton data, available from 1977 onwards, is useful for comparison, since it represents the cosmic ray flux near or at Neptune for some of the time period of interest. However, because of the variable lag of up to 4 months between the time series of neutron monitor data and Voyager 2 data, depending on the position of Voyager 2, we have chosen to focus on data from the Oulu neutron monitor, which has been in continuous operation since the 1960s (ref. 32).
The Oulu neutron monitor detects neutrons generated by primary GCR decaying in the atmosphere. Integrated over the atmospheric column, neutron monitor data is a reasonable proxy for cosmic ray ionization in Earth’s atmosphere (although not necessarily in the lower troposphere15). As the physics of atmospheric ionization is fundamentally similar at Neptune and on Earth11, we use the Oulu data as a source of long-term cosmic ray data. The Oulu neutron monitor is essentially unchanged since installation in the 1960s, but there is an ‘efficiency’ factor applied to the data to include the effects of changes in hardware and software (as well as the routinely applied atmospheric pressure correction). The data are fully explained at http://cosmicrays.oulu.fi/ and in ref. 32. Our analysis uses 1-day averages, although 5-min resolution data is available from 1968.
The Voyager 2 proton data (energy>70 MeV) was obtained by the LECP instrument22, although time series of >70 MeV ions and high-energy alphas and protons from the Cosmic Ray Subsystem instrument33 are similar and could equally have been used. Data (available and described in detail at http://sd-www.jhuapl.edu/VOYAGER/) are sampled at 1 s intervals, but recorded as daily average count rates, with the standard deviations reported. The median standard deviation of these was 0.003 s−1 (with an interquartile range of 0.002–0.004 s−1) compared with a median count rate of 0.072 s−1 that is, a fractional standard deviation of ±4%.
Lyman-alpha ultraviolet data
The Lyman-alpha data is a composite time series of the solar hydrogen 121.57 nm emission line, and represents ultraviolet emissions from the entire solar disc34. It is generated from a combination of satellite measurements and models extending back to 1947, available at http://lasp.colorado.edu/lisird/lya/. For the time period relevant to this paper, the data is taken from the Atmospheric Explorer-E (1977–1980), Solar Mesospheric Explorer SME (1981–1989), the Upper Atmosphere Research Satellite (UARS) SOLSTICE instrument (1991–2000), Solar Radiation and Climate Experiment (SORCE) SOLSTICE instrument (2003–2010) and Solar Dynamics Observatory (SDO) EVE (2010–2015). The times where no satellite data is available (1972–1977 and 2001–2003) are filled in by model calculations35. Detailed discussion of this data set is outside the scope of this paper35, but the uncertainty is estimated to be ±10%.
The periodograms in Fig. 3 were all generated from data selected using an 8-year moving window having a 0.5 cosine bell taper, with steps of 0.5 years between successive data window evaluations. The data were first de-trended to obtain magnitude fluctuations using a loess fit. (The fluctuations were demonstrated to be insensitive to the choice of detrend used in Neptune magnitude data above). The selected data window was cosine tapered (tapering factor 0.5), to reduce the truncation effects of the short data windows. The Lomb–Scargle36,37 approach for irregularly spaced data was used, with the code38 implemented in R. In the case of irregularly spaced data, the minimum detectable period is 2s, where s is the minimum sampling period of the data set. In the Neptune data the minimum sampling interval is 0.7 years, giving a minimum detectable periodicity of 1.4 years (refs 39, 40).
The 1.5–1.9-year periodicity described in the GCR data in the ‘Results’ section was independently confirmed to occur in the 1980s by an additional analysis of the daily GCR data. This analysis used a phase-preserving 1.55–1.81-year Lanczos bandpass filter41 of half-length 8 years, with missing values addressed by multiple bootstrapped realizations14. Computer code is available on request.
Droplet nucleation onto ions in Neptune’s atmosphere
The saturation ratio S required for ions to grow into ultrafine droplets by condensation can be determined using the Thomson equation (2), which describes the equilibrium saturation ratio needed for ion-induced nucleation to become energetically favourable11. In equation 2 r is radius, ρ fluid density, M the mass of the condensing molecule, q charge, γT the surface tension, kB Boltzmann’s constant, T temperature, ɛo the permittivity of free space (all in SI units) and ɛr relative permittivity:
A similar approach was taken to calculate the saturation ratio at which ion-induced nucleation could occur on Neptune9. Here, we apply the Thomson equation for methane and diacetylene (butadiyne), two species thought likely to form droplets through ion-induced nucleation at the pressures and temperatures appropriate for Neptune9. Diacetylene nucleates onto singly charged ions of critical radius 1 nm at a saturation ratio of ∼500, whereas methane needs a saturation ratio of ∼15 for nucleation onto ions (Fig. 7). As these large saturation ratios are expected in the cold Neptune environment9, condensation can occur onto freshly produced ∼1 nm cluster ions. Figure 7 also shows that ion-induced nucleation occurs more easily at lower saturation ratios on multiply charged large ions. For a typical charge of 2e on 10nm particles in Neptune's atmosphere, arising from asymmetry in positive ion and free electron mobilities (ref. 25), estimates of the saturation ratio required for nucleation are ∼100 (diacetylene), and ∼5 (methane), consistent with the ‘relatively efficient’ ion-induced nucleation predicted in ref. 9.
Droplet growth by condensation
We now estimate the rate of droplet growth for methane condensation at 75 K and 1,100 hPa on Neptune with methane saturation ratio of 2.7 in a hydrogen atmosphere9. (There is not enough data available to carry out the calculation for diacetylene).
Following ref. 24, the rate of growth of a droplet of radius r is given by
where, S is the saturation ratio, T is the temperature, L is the latent heat of vapourization, Rv is the gas constant for the condensing species, D is the diffusion coefficient for the condensing species, K is the thermal conductivity, ρv is the vapour density and es(T) is the saturation vapour pressure. Two normalization factors, f(α) and g(β), are also defined24 where,
with p the pressure and R’ the gas constant of the background gas, and α is 1. The second normalization factor is given by
where, 0.02<β<0.04 and is taken here to be 0.04. The terms used in the calculation are listed in Table 3.
Inserting values from Table 3, we find that the estimated droplet growth rate is of order 4 nm s−1, which is insensitive to both the initial radius, and the radius as the droplet grows. This insensitivity to radius arises from the 1/r term in equation 3 being compensated by the r terms in equations 4 and 5.
How to cite this article: Aplin, K. L. & Harrison, R. G. Determining solar effects in Neptune’s atmosphere. Nat. Commun. 7:11976 doi: 10.1038/ncomms11976 (2016).
We acknowledge the diligence and dedication of Dr W Lockwood in maintaining the Neptune observations for over 40 years.
Supplementary Figure 1