Limitations in the chemical characterization of tropospheric organic aerosol (OA) continue to impede attempts to fully understand its chemical sources and sinks. To assess the role of organic nitrates in OA, we used a new thermal dissociation-laser induced fluorescence-based (TD-LIF) technique to obtain a high-time-resolution record of total aerosol organic nitrates (hereafter ΣANsaer) at the Bakersfield, CA supersite during the 2010 CalNex campaign. The TD-LIF measurements compare well with Fourier transform infrared measurements from collocated filter samples. These measurements show that ΣANs are a ubiquitous component of the OA with the –ONO2 subunit comprising on average 4.8% of the OA mass. Scaling this fraction by an estimate of the organic backbone mass yields an estimate that 17–23% of OA molecules contain nitrate functional groups. Measurements of both total ΣAN (gas + aerosol) and ΣANaer show that on average 21% of ΣANs are in the condensed phase, suggesting atmospheric organic nitrates have similar volatilities to analogous non-nitrate oxidized organic compounds. The fraction of ΣAN that is in the condensed phase increases with total OA concentration, providing direct evidence from the atmosphere that absorptive partitioning into OA has some control over the ΣAN phase partitioning. The specific molecular identity of the ΣAN is incompletely understood. Both biogenic hydrocarbons and long chain alkanes are calculated to be significant sources of low volatility nitrates in Bakersfield, and ultra performance liquid chromatography coupled to an electrospray ionization high-resolution quadrupole time-of-flight mass spectrometer measurements confirm the existence of particulate nitrooxy organosulfates derived from gas-phase oxidation of both isoprene and monoterpenes.
 Attempts to predict the relationships between ambient secondary organic aerosol (SOA) concentrations and SOA precursor emissions continue to be challenged in part by limitations in the chemical characterization of organic aerosol (OA). Laboratory experiments have measured aerosol mass yields that result from the oxidation of several organic compounds typically found in the atmosphere [Hallquist et al., 2009], and ambient aerosol has been extensively analyzed with hundreds of molecules being identified [Williams et al., 2010]. However, in the best cases, no more than ~15% of the mass of ambient OA has been specifically identified, thereby limiting our ability to directly assign specific SOA precursors and reaction pathways.
 Recently, functional group and mass spectral analyses of whole aerosol have provided considerable insight into SOA sources and chemistry [Jimenez et al., 2009; Russell et al., 2011]. Despite this progress, the links between specific gas-phase precursors and aerosol concentrations and properties remain tenuous, and several gaps in our understanding are prominent: (1) the role of anthropogenic NOx emissions in controlling SOA mass and properties is not clearly understood [Hoyle et al., 2011], (2) observations that provide a clock for understanding aerosol time evolution show that typically OA is more oxidized than is consistent with gas-phase oxidation rates and mechanisms [Dzepina et al., 2011; Hodzic et al., 2010], (3) correlations between OA and chemical tracers indicate SOA has an anthropogenic origin, yet 14C measurements indicate that the carbon in OA is largely biogenic [Weber et al., 2007], and (4) the generally accepted microphysical model of OA is one that assumes organic particles are liquid and that the hundreds to thousands of compounds in that liquid act as a solvent into which individual molecules partition on the basis of their saturation vapor pressure according to Raoult's law [Donahue et al., 2006; Pankow, 1994; Robinson et al., 2007]. While many laboratory observations support the equilibrium partitioning model, some observations suggest aerosol particles are solid or glassy and thus that gas-aerosol equilibration time scales would be too slow to be the basis for atmospheric modeling [Cappa and Wilson, 2011; Koop et al., 2011]. Additionally, several studies indicate that many SOA compounds are not inert in the condensed phase, and therefore gas-phase chemistry combined with gas/particle equilibrium cannot capture the complete dynamics of SOA processes [Kroll et al., 2009; Lim et al., 2010].
 Understanding the role of organic nitrate (RONO2) functional groups in OA can shed light on these issues. Aside from minor primary sources of short chain nitrates that do not contribute to OA (e.g., methyl nitrate), RONO2 is primarily a result of oxidation of organic compounds in high-NOx environments, providing a unique tracer for SOA produced in anthropogenic plumes [Weber et al., 2007]. Nitrate functional groups are primarily derived from anthropogenic emissions of nitric oxide (NO); thus, aerosol that incorporates these groups will correlate with tracers of anthropogenic emissions even if the carbon backbone is biogenic [Perring et al., 2013].
 In the laboratory, oxidation of medium-sized (C5–C9) organic molecules that are important in the atmosphere shows that chemical production of alkyl and multifunctional nitrates forms aerosol in moderate yields for chemistry initiated by both the NO3 radical [Ng et al., 2008; Rollins et al., 2009] and by OH [Lim and Ziemann, 2005; Matsunaga and Ziemann, 2008]. In many chamber studies, high-NOx conditions and therefore RONO2 formation suppress the higher yields of alternative aerosol formation mechanisms [Kroll et al., 2006; Ng et al., 2007]. For C10 and larger molecules, chamber observations and structure-activity relationships [Pankow and Asher, 2008] indicate that adding –ONO2 functional groups reduces the vapor pressure of the reaction products to a point where they partition significantly into the condensed phase and two or more oxygen-containing functional groups put the molecules almost exclusively in the condensed phase.
 In contrast to these laboratory observations, for ambient aerosol, it has been difficult to characterize the role of –ONO2 functional groups. Many traditional techniques and some state-of-the-art methods for aerosol analysis are generally unable to discriminate between organic and inorganic nitrate (e.g., NOy detection and aerosol mass spectrometers). However, recent applications of chemical instrumentation including Fourier transform infrared (FTIR), liquid chromatography/electrospray ionization-mass spectrometer (LC/ESI-MS), ESI-MS, and aerosol mass spectrometer (AMS) have established the importance of multifunctional organic nitrates in atmospheric OA [Day et al., 2010; Farmer et al., 2010; Nguyen et al., 2011; O'Brien et al., 2013; Surratt et al., 2008].
 Here we apply a new technique that uniquely detects aerosol organic nitrate. We observe the total of gas and particulate RONO2 (ΣAN) using thermal dissociation-laser-induced fluorescence (TD-LIF), and simultaneously the particle only RONO2 (ΣANaer) using TD-LIF in combination with a gas-phase denuder [Rollins et al., 2010]. The measurements are made with high-time resolution (~5 min) allowing us to examine the variability in aerosol composition on the time scales of fluctuations in source composition and chemistry. In a recent publication [Rollins et al., 2012], we discussed nighttime observations that demonstrate the importance of nitrate radical chemistry as a SOA source. In this work, we use the daytime observations to observe the OA mass (COA) dependence of the RONO2 partitioning into aerosol in the atmosphere and to constrain the saturation concentration (C*) distributions of the ambient nitrates.
2.1 CalNex SJV Site
 The measurements reported here were collected at the CalNex 2010 San Joaquin Valley (SJV) site in Bakersfield California during 15 May to 29 June 2010. Bakersfield is located at the southern end of the SJV, which is one of the most productive agricultural regions in the United States. The region has extensive lands devoted to cattle raising and active oil and natural gas drilling and processing industries. The CalNex SJV site was located at 35.3463°N –118.9654°W, which is approximately 6 km southeast of the Bakersfield city center. A busy commuter freeway lies 0.75 km to the north of the site. The prevailing winds in the morning were typically from the southwest at ~5 km/h. Throughout the day the winds gradually increased and shifted to the northwest with an average daily maximum speed of 15 km/h [Ahlm et al., 2012]. A map of the SJV and location of the measurement site with typical daytime wind direction is shown in Figure 1.
2.2 TD-LIF Instruments
 Measurements of ΣAN and ΣANaer were conducted using TD-LIF [Day et al., 2002; Wooldridge et al., 2010]. This was the first field deployment of the ΣANaer measurement [Rollins et al., 2010]. The TD-LIF instruments detect ΣAN by sampling air through a heated quartz inlet tube into an LIF-based NO2 detector. The inlet temperature is typically held near 320°C where all organic compounds of the form RONO2 decompose in the gas phase quantitatively yielding RO + NO2. The specifics of the system used in this study to make the ΣAN measurements are described by Day et al. , and an intercomparison with independent measurements of speciated gas-phase RONO2 is described by Beaver et al. .
 The ΣANaer measurements were made using the instrument described in Rollins et al. . In this instrument, LIF of NO2 was accomplished by excitation at 408 nm using a 30 mW single-mode continuous-wave diode laser (Power Technology). Red-shifted fluorescence photons were detected at wavelengths long of 650 nm using a photomultiplier tube module (Hamamatsu H7421-50). Scattered photons were filtered from the signal using a stack including one each colored glass (Schott) and dielectric (Barr) 650 nm long pass filters. A 38 pass White Cell, identical to that used in Thornton et al. , was employed to achieve the desired signal:noise, which typically resulted in a 19 pptv detection limit for one minute of averaging.
 The ΣANaer instrument uses an activated carbon denuder (MAST Carbon, U.K.) to remove gas-phase NOy (NOy = NO + NO2 + NO3 + RONO2 + 2 x N2O5 + ClNO2 + …) from the sample flow before entering the heated section of the inlet, where particles are evaporated and RONO2 is converted quantitatively to NO2. The difference between the instrument used here and that described by Rollins et al.  is primarily in the denuder used to remove gas-phase NOy. For this study, we used a more efficient multichannel denuder that was 2.2 cm in diameter and 10 cm long (MAST Carbon, UK). The channels comprised 44% of the cross-sectional area of the denuder, which with the 500 sccm flow rate resulted in a transit time of 1.9 s through the denuder. At ambient temperatures, this resulted in an insignificant evaporative loss of semivolatile particles. A dry PM2.5 cyclone was used to remove large particles before air entered the denuder. An automated stainless steel ball valve (Swagelok) was used to periodically bypass the denuder and flow NO2 calibration standards into the instrument. Measurements of the instrument's zero response were made by overflowing the inlet through the denuder with zero air. Both the zero and calibration constants had regular diurnal variations on the order of 10% due to changes in laser alignment resulting from temperature changes in the trailer that housed the instruments. Measurements of the instrument's calibration constant were performed hourly and zero measurements every 30 min. These were sufficient to observe all significant variations in the instrumental characteristics and maintain high accuracy without significantly reducing the duty cycle (duty cycle ~90%).
 The TD-LIF inlets were located on a scaffold tower with the ΣANaer inlet at 5.5 m above ground level, and the ΣAN inlet at 15 m. During the day, observed gradients in NO2 between the two heights were small, while at night, the two heights often sampled distinct air masses with 10–20% higher NO2 aloft. At each inlet, the sample flow passed through a critical orifice that reduced the pressure to <60 hPa. The transit time from that point through 3.2 mm ID tubing to the detector is less than 10 ms, keeping the potential for chemistry to affect NO2 before detection to a minimum [Wooldridge et al., 2010].
 The accuracy of the TD-LIF measurement of ΣANaer is determined by the efficiency of the removal of gas-phase NOy compounds, the transfer function for particles through the denuder and into the heater, the efficiency with which particulate nitrates are converted to NO2, and the accuracy of the NO2 measurement. These issues are discussed in detail by Rollins et al. . Of most concern, is evaporative loss of particles in the denuder. To constrain this term, we calculate the upper limit to evaporative loss assuming evaporation without condensation. Compared to our original work where we used a denuder residence time of 9.3 s for this calculation, here we set the residence time to 1.9 s by a combination of denuder and flow rate. This is sufficiently long to fully remove gas-phase NOy and reduce the potential evaporation of aerosol by an additional factor of 4.9 [Rollins et al., 2010]. Using the transmission efficiency reported in Rollins et al. [2010, supporting material] and the SMPS measurements of the size distribution of the aerosol at Bakersfield, we calculate a mean transmission efficiency through our inlet of 93% (the 7% loss is due to thermophoretic deposition at the heater entrance), and a transmission of better than 90%, for more than 7/8 of the measurements during CalNex.
 Mixing ratios of NO2 resulting from the thermal decomposition of RONO2 are converted to mass concentrations of the nitrate functional group in air using the number density of air and the molecular weight of the nitrate group (62 g mol−1). At standard conditions (1013 hPa, 298 K), this factor is 2.53 µg m−3 ppb−1. The instrument typically had a background count rate near 500 counts per second (CPS) due to scatter of laser light in the LIF cell and a sensitivity to NO2 of 150 CPS ppb−1. For one minute of measurement, this results in a theoretical detection limit (1σ noise at a concentration of zero, [Thornton et al., 2000]) of 0.019 ppb. Concentrations at the site were low; thus, the distribution of differences between adjacent points in the time series (ppb at time t + 1 min – ppb at t) for all data is expected to be a normal distribution with an approximate width (2σ) of 0.038 ppb. A Gaussian fit to the distribution has a width of 0.0395 ppb, in good agreement with the expected noise level. Converting this measurement of mixing ratio to mass of particulate ΣAN gives a detection limit of 48 ng m−3.
 A potential interference for the TD-LIF ΣANaer measurement is particulate peroxy nitrates (PNs), which would also be detected. These compounds are not expected to contribute significantly to particulate concentrations since their short thermal decomposition lifetime should result in rapid losses in the condensed phase. For example at 300 K and 1013 hPa in the gas phase, the lifetime of peroxyacetyl nitrate (PAN) to decomposition is 22 min. For particle phase PNs, this lifetime would be expected to be an upper limit due to the absence of NO2 with which gas-phase PAN exists in equilibrium and the more rapid thermal transfer in the condensed phase which may further decrease PN lifetimes.
 A primary advantage of TD-LIF is that ammonium nitrate (NH4NO3) is not detected by the instrument due to the significantly higher enthalpy change for the thermal decomposition of HNO3 (206 kJ mol−1) as compared to RONO2 (e.g., 151 kJ mol−1 for CH3ONO2, [Gray et al., 1981]). Laboratory tests have shown the instrument to be insensitive to NH4NO3 when the inlet is held near 320 °C as was done here. The measurements from Bakersfield yield confidence in this as ΣANaer was more highly correlated to OA than it was to aerosol NO3(-) even though aerosol NO3(-) was typically ~10 times ΣANaer (see Figure 5 and section 4).
2.3 Additional Particle Measurements
 Measurements of PM1 OA concentrations were made using an Aerodyne high-resolution time of flight AMS as described in Liu et al. [2012a]. Measurements of organic functional groups including RONO2 were made by FTIR analysis of filter samples [Day et al., 2010; Liu et al., 2012a]. Typically, FTIR organonitrate group mass has been reported to include the associated fraction of C mass (6 g mol−1 of C for a total of 68 g mol−1 for organonitrate), but here, all TD-LIF and FTIR organonitrate group mass are reported using 62 g mol−1 for consistency. Both (dried) PM1 and PM2.5 samples were collected using FTIR, and typically 83% of the PM2.5 RONO2 mass was found to be in PM1. Both the AMS and filter samplers used inlets on the top of a trailer located next to the sampling tower at the same height as the TD-LIF ΣANaer measurements. Volatile and intermediate volatility organic compound (VOC, IVOC) measurements on the tower were made by gas chromatography with mass spectral and flame ionization detection [Gentner et al., 2012].
 A number of isoprene and monoterpene oxidation products in the condensed phase were measured using ultra performance liquid chromatography coupled to an electrospray ionization high-resolution quadrupole time-of-flight mass spectrometer (UPLC/(-)ESI-Q-TOFMS) operated in the negative (–) ion mode [Surratt et al., 2008]. Many of the measured compounds were nitrooxy organosulfates. Details of UPLC/(-)ESI-Q-TOFMS operating conditions and procedures can be found elsewhere [Zhang et al., 2011]. High-volume filter samplers operating at 226 L min−1 with PM2.5 inlets were used to collect fine aerosol onto prebaked 86 cm2 quartz fiber filters. The samples were collected daily from 12 A.M. to 11 P.M. (local time), resulting in 38 individual 23 h filter samples. Field blanks were collected weekly by placing prebaked quartz fiber filters into samplers for 15 min before removing and storing in the same manner as the PM2.5 filter samples. All UPLC/(-)ESI-Q-TOFMS filter samples collected during the campaign were shipped frozen to the laboratory. Upon arrival to the laboratory, all samples were stored in a freezer at –18 °C until time of analysis. Before UPLC/(-)ESI-Q-TOFMS analyses, filter samples were extracted using the detailed procedures outlined in Zhang et al. [Zhang et al., 2012]. Field and lab blanks were treated similarly to the PM2.5 filter samples. No OA constituents detected from the PM2.5 filter samples were seen in these blanks, indicating that nitrooxy organosulfates detected by this technique were not introduced during sample storage or preparation.
 Nitooxy organosulfates derived from isoprene and monoterpenes were identified based on comparison to prior work by Surratt et al. [Surratt et al., 2008]. Specifically, retention times, accurate mass data, and MS/MS spectra were used to confirm the identity of these compounds. None of the nitrooxy organosulfates detected in the PM2.5 samples have commercially available standards for quantification. As a result, calibration curves of propyl sulfate (City Chemical, 98% purity), octyl sulfate (Sigma, 99% purity), and decyl sulfate (Fluka, 99% purity) were generated for use as surrogate standards. These three compounds all contained an organosulfate group (R-OSO3); therefore, their response factors during UPLC/(-)ESI-HR-Q-TOFMS analyses were assumed to be similar to those of the measured nitrooxy organosulfates derived from BVOC oxidation. One of these surrogate standards was chosen to quantify the observed nitrooxy organosulfates from Bakersfield on the basis of retention time and structural similarity (i.e., similar carbon numbers). The approximate identified organonitrate mass from the UPLC/(-)ESI-Q-TOFMS analyses was calculated by scaling the derived organic mass by the mass of the nitrate functional group/compound MW. Significant uncertainties are associated with quantification of these compounds using UPLC/(-)ESI-Q-TOFMS due to variable response factors depending on the compound and the solvents present during ESI analysis [Cech and Enke, 2001; Surratt et al., 2008].
3 Comparison of Particle RONO2 Measurements
 A unique aspect to the instrumentation at the CalNex SJV was that three independent techniques were used for simultaneous measurements of particulate organic nitrates. The PM1 FTIR samples were typically collected for between 3 and 6 h each. PM2.5 samples used for UPLC/(-)ESI-Q-TOFMS analyses were collected for 23 h (12 A.M. – 11 P.M.). TD-LIF measurements were collected at 1 Hz and typically above the detection limit for a 1 min average. All three data sets averaged to the UPLC/(-)ESI-Q-TOFMS time resolution are shown in Figure 2. The total mass of particulate organonitrate measured by UPLC/(-)ESI-Q-TOFMS mass is of order 1% of the other two due to the unavailability of available authentic standards and inability to ionize nonacidic organonitrate constituents. Nonetheless, the UPLC/(-)ESI-Q-TOFMS measurements were somewhat correlated to ΣANaer (r = 0.36), indicating that the measured compounds are representative of important ΣANaer sources.
 Figure 3 shows the TD-LIF measurements averaged to the FTIR time resolution and regressed against the FTIR data. For this comparison, we have adjusted the TD-LIF data down by a factor of 0.83 to adjust for size cut differences between the instruments (RONO2 PM1/PM2.5 [Liu et al., 2012a]). A linear fit to the data yields an offset of 0.068 µg/m3 and a slope of 1.38 (i.e., slope implies FTIR is 28% below TD-LIF). A good correlation was observed (r = 0.72); however, Figure 3 shows that the TD-LIF instrument almost always measured more ΣANaer than the FTIR. The cause(s) of the differences are not obvious, and both research groups rechecked their calibration and other possible sources of positive or negative bias. For the TD-LIF instrument because of the presence of exceptionally high levels of NH3 and NH4NO3 in Bakersfield, we rechecked and confirmed that the instrument is insensitive to these compounds. For the FTIR measurement, samples were dried and frozen, then analyzed 1–2 months later at moderate humidity (<40%). Evaporative loss of nitrates from the filters prior to FTIR analysis is known to occur to some degree, and is challenging to quantify [Day et al., 2010; Liu et al., 2012b]. Due in part to these recognized challenges in these measurements, the stated uncertainty is 20%. The observed difference of 28% would represent losses that are somewhat higher than expected, although the FTIR OA was also 30% below the AMS OA. Comparisons of the FTIR 24 h samples and integrated 3–6 h samples provide evidence that significant losses are not associated with longer sampling times [Day et al., 2010]. Despite the measurement differences, the comparison between the two data sets provides good evidence that both techniques quantify ΣANaer and puts bounds on the absolute concentration that are of order ±25% from the mean of the two measurements.
4 ΣANaer Observations
 The TD-LIF measurements show that ΣANaer is an important fraction of both ΣAN and OA. In Figure 4, daytime measurements of ΣANaer are plotted against ΣAN (10 min means). The linear fit to this data (r = 0.43) shows that during the day, on average 21% of ΣAN is in the particle phase, although there is real variability in this fraction that exceeds the precision of the measurements and is likely due to variations in the chemical identity of the ΣAN molecules. Finding 21% in the condensed phase provides insight into the volatility distribution of the large group of organic compounds comprising ΣAN. As a point of reference, given the typical OA concentrations observed in Bakersfield (~5 µg m−3), compounds existing in the condensed phase via absorptive partitioning must have vapor pressures (Pvap) lower than ~10−4 Pa. Only very large (~C15 and larger) monofunctional nitrates are expected to have vapor pressures this low. As a rough estimate, vapor pressures are reduced by a factor of 100 by the addition of hydroxyl or carbonyl groups [Pankow and Asher, 2008], and thus given one to two additional functional groups, nitrates with 5–10 carbon are expected to be found in SOA. Given that almost all of the molecules comprising ΣAN are expected to have less than 15 carbon atoms (See section 6 and Figure 6), this is strong evidence that a large fraction of the organic nitrates in Bakersfield contain two to three oxygen-containing groups and are likely products of two to three oxidation reactions.
 In Figure 5, comparisons of ΣANaer to the AMS PM1 measurements are shown. Of the aerosol chemical components measured in Bakersfield, we find that ΣANaer is correlated the most strongly with the AMS OA (r = 0.58). This suggests that ΣANaer has a similar source to that of other OA, which at this site is dominated by SOA from gas-phase oxidation primarily of anthropogenic VOCs [Liu et al., 2012a]. The correlation with inorganic nitrate (r = 0.43) and with the inorganic ion balance (molar ratio of 2 × SO4(2−) + NO3(−) + Cl(−) / NH4(+), r = 0.06), a surrogate for particle acidity, was weaker. These observations differ from those of Day et al.  who reported observations in coastal southern California with important source regions identified as Riverside and the South Coast Air Basin. Those measurements showed strong correlations between ΣANaer and inorganic NO3(-) as well as with the product of AMS organics and NO3(-) suggesting that similar conditions favored the formation of ΣANaer and inorganic particulate nitrate. The observed relationships between ΣANaer and inorganic aerosol compounds may differ between this work and that of Day et al.  for multiple reasons. One possibility is that heterogeneous chemistry plays different roles in controlling ΣANaer in the two locations. The ammonia in Bakersfield was quite high, and consequently Figure 5 shows that the particles were almost always neutralized (molar ion ratio typically ≤1), whereas the observations by Day et al.  show this ratio typically greater than 1. Although acidic aerosol was reported to be correlated with low ΣANaer by Day et al. , this was not the case in Bakersfield, and thus acid-catalyzed hydrolysis does not appear to be an important process controlling ΣANaer content for the majority of the aerosol that were observed in this work. The generally low RH in Bakersfield (nighttime mean high, 60%, daytime mean low, 21%, Figure 8) as compared to source regions in that study (nighttime mean high, 70%, daytime mean low, 45%) may play a role in reducing the importance of nitrate hydrolysis. This argument may be supported by a weak anticorrelation between RH and ΣANaer observable in Figure 2 although the relationship between RH and ΣANaer was not consistent enough for us to draw a strong conclusion in this regard. Other possibilities are differences in chemical regime associated with different correlations between VOC and NOx or absolute levels of VOC and NOx in the two locations.
 On average, in Bakersfield, the ΣANaer mass (nitrate fragment only) was 4.8% of OA. Given the difference between TD-LIF and FTIR ΣANaer (TD-LIF 38% higher) the nitrate mass fraction could be as low as 3.5% of PM1 OA (AMS OA uncertainties are also ± 30% and not considered here). If we assume a molecular weight of the ΣANaer of 300 g-mol−1 (See section 5 and Figure 7), then this translates to 17–23% of the OA mass assigned to molecules with an –ONO2 subunit.
5 ΣANaer Sources Molecules
 The large fraction of OA that is organic nitrate molecules implies that understanding the chemical sources of ΣANaer will shed light on the sources of OA and provide some indication of the effectiveness of possible strategies for reducing SOA. As an extreme, one can speculate that eliminating the source of ΣANaer would result in reducing OA by at least 17%. Such a reduction could come about either by eliminating the NOx that is incorporated into the organic molecules that form the OA or by eliminating the organic precursors. To assess the potential for such strategies, we need more detailed knowledge of the molecular composition of ΣANaer. While the TD-LIF and FTIR measurements do not provide such information, we can combine the insight from the specific measurements of molecular constituents in the SOA from the UPLC/(-)ESI-Q-TOFMS with a calculation of AN formation rates and Pvap based on the observed VOC at the Bakersfield site.
 Alkyl and multifunctional nitrates in a continental location such as Bakersfield have essentially no primary sources. The weak sources associated with intercontinental transport of directly emitted nitrates carry molecules with vapor pressures that are too high to be incorporated into aerosol (e.g., methyl nitrate). Therefore, ΣANaer is likely to only have local sources from gas-phase oxidation of locally emitted VOCs, involving multigeneration chemistry that results in adding functional groups to a nitrate or a nitrate group to a functionalized molecule [e.g., Rollins et al., 2009], and possibly from chemistry in the condensed phase such as nitration of epoxides in acidic conditions [Eddingsaas et al., 2010; Hu et al., 2011]. Aqueous-phase chemistry may also result in hydrolysis of organic nitrates converting the nitrogen to HNO3 [Roberts, 1990; Hu et al., 2011; Liu et al., 2012b].
 In the gas phase, nitrates are produced by oxidation of organic molecules in the presence of NOx. During the day, the primary source is the reaction of photochemically produced organic peroxy radicals (RO2) with NO, which can result in the formation of a nitrate, or an organic oxy radical and NO2.
 In the presence of oxygen, channel R1b will be followed either by a reaction with O2 resulting in carbonyl formation,
or an intermolecular isomerization or decomposition. During nighttime, sources of hydroxyl radicals (OH) are nearly absent, but a significant channel to form RONO2 exists due to the reaction of nitrate radicals (NO3) with olefins. The yield (α) of RONO2 for a given compound/oxidant combination is the fraction of the RO2 + NO, or R = R′ + NO3 reactions which yield RONO2. Through (R1) the yields of RONO2 are low for small organic compounds (a fraction of a percent for CH3O2) and increase with carbon number to a limiting yield near 35–40% for C8–10 peroxy radicals [Arey et al., 2001; Atkinson et al., 1982; Carter and Atkinson, 1989]. Key species in many locations are biogenics, such as isoprene, which has a net yield (multiple RONO2 isomers) of 12% ± 3% [Paulot et al., 2009; Sprengnether et al., 2002] and monoterpenes such as α-pinene (~18% yield [Nozière et al., 1999]). Yields for NO3 initiated oxidation are much higher (>50%), and nighttime production of ΣANs may approach 50% of the daytime production rate [Fry et al., 2013].
 We use the VOC measurements in Bakersfield, weighting these by their reactivities towards OH or NO3, and yields to form AN to calculate an estimate of the relative importance of different primary VOC as chemical sources of ΣANaer. There is relatively little time of day variation in the calculated daytime or nighttime fractional importance of the AN sources, and thus we show in Figure 6 two pie charts representing the contributions of VOC to production of ΣANaer initiated by OH (daytime) and NO3 (nighttime). Tables 1 and 2 in the supporting information provide the details of the calculations. The compounds that are important are not the same compounds that are important to O3 production or to total OH reactivity.
 During the day, the dominant source of nitrates is calculated to be moderate to large anthropogenic alkanes, which are known to have high AN and SOA yields [Lim and Ziemann, 2005] and alkenes. Anthropogenic VOC emissions were also concluded by Liu et al. [2012a] to be the major SOA source at this site. Terpenes including α-pinene and d-limonene are also an important source of nitrates, and these are known to have low Pvap. Isoprene was a significant contributor to primary AN production. Multigenerational chemistry has been shown to produce significant SOA from isoprene, and isoprene oxidation products, such as the nitrooxy organosulfates, have also been previously observed in ambient SOA [Claeys et al., 2004; Surratt et al., 2008]. We only include the first generation in these calculations.
 The UPLC/(-)ESI-Q-TOFMS data provide additional evidence that monoterpenes and multiply oxidized isoprene products are important to the organic nitrate fraction of the aerosol. A number of specific nitrooxy organosulfates were observed; these included two derived from isoprene oxidation observed at m/z 260 (C5H10NO9S−) and 305 (C5H9N2O11S−) as well as eight derived monoterpene oxidation observed at m/z 294 (C10H16NO7S−), 296 (C9H14NO8S−), 310 (C10H16NO8S−), 312 (C9H14NO9S−), 326 (C10H16NO9S−), 328 (C10H18NO9S−), 330 (C9H16NO10S−), 342 (C10H16NO10S−), and 373 (C10H17N2O11S−). All of these nitrooxy organosulfates can be generated from isoprene and monoterpene oxidation by either OH under high-NOx conditions or by NO3, both in the presence of acidified sulfate aerosols [Surratt et al., 2008].
 The three most abundant (i.e., m/z 305, 294, and 296) of these are shown in Figure 7. Interestingly, these most abundant ions have been demonstrated to form from isoprene (m/z 305), α-pinene (m/z 294), and d-limonene (m/z 296) oxidation [Surratt et al., 2008], consistent with their importance to contributing to the AN production shown in Figure 6, especially at night. The total mass of ΣANaer estimated from the UPLC/(-)ESI-Q-TOFMS observations is on average 0.4% of the TD-LIF ΣANaer. One reason for the low fraction of ΣANaer observed by UPLC/(-)ESI-Q-TOFMS is that this technique is only sensitive to organic compounds containing acidic functional groups, such as organosulfates, which efficiently deprotonate during the ESI process and are detected in the negative ion mode as [M – H]– ions. The exact mechanisms for nitrooxy-organosulfate formation remain unknown [Surratt et al., 2008], but there are no known mechanisms in the gas phase to produce these compounds. These compounds likely form through heterogeneous chemically pathways and warrant further investigation. Due to the low RH and particle acidity in Bakersfield, the aqueous-phase reactions forming sulfates are expected to be slow there, and thus, most of the ΣANaer molecules probably do not have these groups that make them detectible using this technique. Further, while hydroxynitrates are a significant oxidation product of alkenes, this is not the case for alkanes, and thus this potentially significant subset of ΣANaer due to alkanes may not be detectable using existing techniques.
6 Gas/Particle Partitioning of ANs
 Absorptive partitioning theory based on Raoult's law postulates that the fraction of each organic compound that is found in the condensed phase increases with the mass of absorbing (solvating) aerosol (COA). For atmospheric organic species, the chemical identity of COA has been suggested to be total OA. In the case of water-soluble organics, condensed phase liquid water has also been suggested to serve as the solvent. In either case, if absorptive partitioning theory is correct, then the equilibrium fraction of a specific compound found in the condensed phase (Yi) is described by equation ((1)).
 Here, Ci and Ci,p are, respectively, the total and particle phase concentrations of species i, and Ci*(T) is the temperature-dependent saturation concentration of species i. In this theory, the equilibrium variations in the partitioning of a specific compound are only due to changes in COA or T [Donahue et al., 2006; Pankow, 1994].
 Figure 8 shows average diurnal profiles of ΣAN, ΣANaer, AMS OA, ambient temperature, as well as the mass fraction of OA that was nitrate and the fraction of ΣAN in the condensed phase over the time range 15 May to 29 June 2010. We show only the daytime measurements (7 AM – 5 PM) that are used in the following analysis. The observed increase of ΣAN was strongest in morning (8 AM – 11 AM). However, the largest concentrations of ΣANaer were observed later in the day, coincident with an increase in the total OA. The ΣANaer contribution to total OA was highest in the early morning and steadily decreased throughout the day. This observation is explained by the differences between nighttime VOC oxidation, which is dominated by nitrate radical leading to high yields of organic nitrates, and photochemistry which generally has lower yields of ANs [Rollins et al., 2012]. The fraction of ΣAN in the condensed phase increased in the afternoon, indicating decreases in ΣAN volatility and/or partitioning to the condensed phase due to an increase in COA.
 Analysis of the variability in the ΣANaer/ΣANtotal (Ytot) data indicates that temperature and RH have a weak or nonobservable effect on the gas/particle partitioning of ΣAN over the ranges sampled. In contrast, total OA mass does have an observable influence on Ytot. Larger concentrations of OA are associated with an increase in the fractions of ΣAN in the aerosol phase (Figure 9), as is expected from absorptive partitioning.
 To determine the volatility distribution of organic nitrates, we analyze the data assuming absorptive partitioning controls the fraction of ΣAN in the condensed phase. Here we presume that the observed COA dependence of the fraction of total organic nitrates in the particle phase (pΣAN / ΣAN = Ytot) can be reproduced using a finite number of surrogate compounds of varying Cj*.
 We explicitly distinguish the real compounds (i) from surrogate compounds (j). Fj is the fraction of ΣAN that can be represented as having a saturation concentration Cj* and thus . The two product model for example [Odum et al., 1996] is equivalent to equation ((2)) where n = 2.
 Figure 9 shows Ytot (10 min average of ΣANaer / 10 min average of ΣAN) plotted against M0 and equation ((2)) with varying n was used as a fitting function. Because ΣAN is in the denominator of Ytot, the analysis is especially sensitive to noise in this parameter. The ΣAN measurement is made by subtracting the sum of NO2 and peroxynitrates measured in one instrument channel from the sum of these plus ΣAN measured with another channel [Day et al., 2002]. Therefore, the ΣAN quantity was frequently quite noisy due to very high (>100 ppb) and rapidly changing NO2. The particle ΣAN channel is much less noisy since NO2 is removed with the denuder. As a result, ΣANaer was measured more precisely than ΣANtotal even though the concentrations of the aerosol organic nitrate were lower.
 Equation (2) has been used throughout the literature to fit data in two different ways. The so-called two product model uses equation ((2)) with n = 2, and both Fj and Cj* are used as fitting parameters. More recent publications have followed Donahue et al.  using the so-called volatility basis set approach where the Cj* are fixed and logarithmically spaced and only the Fj are used as fitting parameters. Typically, four C* values have been sufficient to fit the data, and so both methods frequently result in four fitting parameters. We have fit our data with both the two product model and the volatility basis set using various basis sets. Using the two product model, the best-fit parameters were: F1 = 0.34, C1* = 0.73, F2 = 0.66, C2* > 100. Here we state C2* as having a lower limit of 100 because we cannot constrain an upper on the value of C2* given that the OA concentration of our measurements did not significantly exceed 10 µg/m3. This essentially means that 66% of the organic nitrates are too volatile to condense under any ambient OA loadings in Bakersfield. Using the volatility basis set approach, we tried using basis sets spanning the range 10−1 – 103. The best fit uses C1* = 0.1, F1 = 0.04, C2* = 1, F2 = 0.30, C3* > 100, F3 = 0.66. Both fitting approaches are shown in Figure 9, and it is clear that there is virtually no difference in the quality of fit. To illustrate the significance of the fit, we also show in Figure 9 two partitioning curves assuming that 66% of the OM is completely volatile, and the remaining 34% has a single C* value of 0.1 or 10.
 The fit to the data in Figure 9 demonstrates that under ambient conditions with moderate OA concentrations, typically ~20% of ANs are in the condensed phase and that at OA concentrations above 10 µg/m3 as much as 34% will condense. This is significantly more than would be expected from the chemistry captured by a calculation of the distribution of vapor pressures of first generation oxidation products of the measured AN precursors. To illustrate this point, we used the SPARC model [Hilal et al., 2003] to estimate vapor pressures of the nitrates generated from the known sources in Bakersfield as indicated in Figure 6. For each precursor, a representative nitrate product was used to estimate the vapor pressure of the class of products. The SIMPOL model [Pankow and Asher, 2008] was also used to calculate vapor pressures for many compounds, and SIMPOL and SPARC agreed within a factor of 2–3. Vapor pressures were converted to C* values assuming an average MW for OA of 200 g/mol. Using these saturation concentrations, less than 1% of ΣAN is predicted to be in the condensed phase under all observed M0 conditions. A uniform decrease in vapor pressure of all nitrates of 104–105 is required to calculate, respectively, 19–28% of the nitrates in the condensed phase at 3 µg/m3 (a typical OA concentration, Figure 8). This suggests that nitrates have undergone approximately two additional stages of oxidative chemistry beyond the initial VOC + OH reactions. This is of course a gross simplification since we have done the calculation assuming that all compounds are reduced as opposed to increased in volatility through atmospheric oxidation. However, the same result is achieved if we only reduce the volatility of those compounds that start with at least nine carbons (and isoprene). All smaller compounds even after a reduction in vapor pressure by a factor of 105 still have C* values greater than 40 µg/m3, meaning that they do not significantly contribute to particles. The finding that ~2 generations of oxidative aging are required to explain the observations of AN volatility is in good qualitative agreement with a number of recent studies that have estimated the volatility and age of atmospheric OA [e.g., Hildebrandt et al., 2010; Jimenez et al., 2009; Russell et al., 2011].
7 Discussion and Conclusions
 A new technique was used to successfully quantify ambient total particulate organic nitrates with higher time resolution and precision than previously reported techniques. The data compare well with those from colocated FTIR filter measurements.
 Nitrates were found to be ubiquitous in the OA in Bakersfield, with on average 4.8% of the mass being from this moiety during the day. Calculations suggest that the most significant sources of the nitrated OA molecules are gas-phase oxidation of both biogenic hydrocarbons and long-chain anthropogenic alkanes. Isoprene and monoterpene oxidation products containing one to two nitrate groups were chemically characterized in the condensed phase using UPLC/(-)ESI-Q-TOFMS, and the dominant compounds from monoterpenes measured had one nitrate group and total molecular weights near 300 amu (Figure 7). For these compounds, the nitrate mass fraction is ~20%. In the case of the detected isoprene oxidation product with two nitrate groups, it had a molecular weight of 306, resulting in a nitrate mass fraction of 40%. If these molecules represent typical nitrated SOA, then we calculate that on the order of 17–23% of OA molecules are organic nitrates.
 Bakersfield is a high NOx environment meaning that almost all organic peroxy radicals produced during the day react with NO, eventually forming either a nitrate, an alcohol, or a carbonyl. Our observation that ~17–23% of SOA molecules contain nitrate groups is comparable to the yields to form nitrates in the gas phase from molecules large enough (>C4) to form SOA (i.e., α, section 5 and Table 2 in SI). This is suggestive that the product channel following the RO2 + NO reaction does not have a significant control over the SOA yield (i.e., fraction of gas-phase oxidation products that are nitrates ≈ fraction of SOA molecules that are nitrates). This suggests that nitrates have a similar volatility and condensed-phase stability to other SOA forming molecules, a result similar to one we found in a laboratory study [Rollins et al., 2010]. This conclusion is consistent with the similar vapor pressure changes expected from the addition of these different functional groups to a molecule [Pankow and Asher, 2008]. Thus, our measurements would suggest that if NOx has a significant impact on photochemical SOA formation in the atmosphere, it is likely due to an acceleration of photochemistry, or fragmentation of hydrocarbon backbones as opposed to which functional group quenches the organic radical. In this work, we did not see evidence that condensed-phase hydrolysis or acidic chemistry played a major role in determining nitrate concentrations.
 The simultaneous measurements of ΣANaer and ΣAN allowed us to observe that the gas/particle partitioning of nitrates is a function of total OA, in agreement with equilibrium partitioning theory. We also observe an additional time of day dependence of ΣANaer/ΣAN (Figure 8). Because we could not see a direct relationship between all of the ΣANaer/ΣAN and temperature data, we conclude that the diurnal variability in ΣANaer/ΣAN is most likely due to chemistry, with increases in this ratio late in the day probably due to the production of more highly oxidized and condensable compounds. These measurements also allowed us to constrain the effective saturation concentration distribution of the nitrates in ambient OA, under the assumption of equilibrium partitioning. Thus far, saturation concentrations for ambient OA have only been quantified indirectly using thermaldenuders [Cappa and Jimenez, 2010; Huffman et al., 2009; Lee et al., 2010]. We find that approximately one third of the nitrates have saturation concentrations on the order of 1 µg/m3. This is significant because typically OA concentrations in Bakersfield are near this level, and therefore SOA appears to potentially have an important positive feedback on itself in this location.
 The results presented here for organic nitrates exhibit strong parallels to those shown by [Hennigan et al., 2009] who described gas/particle partitioning of total water-soluble organic compounds (WSOC). On average, Hennigan et al.  found that 24% of WSOC was in the condensed phase, compared to our observed 21% of ΣAN being condensed. They observed that the fraction of WSOC in the condensed phase increases with the particulate WSOC (WSOCp), but does not increase with total OC (measured using a Sunset Labs EC/OC analyzer). This suggested that a significant fraction of OC is not soluble in water and that the activity coefficients of WSOC in this nonwater soluble OA deviate significantly from one. Nevertheless, Hennigan et al.  observed very similar partitioning behavior with respect to WSOCp concentrations that we observed for ΣAN with respect to the AMS OA. There, WSOCp partitioning increased up to WSOCp concentrations of ~4μg/m3 above which a plateau was observed, suggesting the C* values for WSOC are effectively within a factor of 2–3 of those derived in this work for ΣAN. While Hennigan et al.  have observed that high RH and particulate water enhance partitioning of WSOC to the particle phase, we did not observe any trend in ΣAN partitioning with RH. However, this may be only due to the lack of high RH observations in Bakersfield. Very few episodes of RH higher than 70% were observed there, where Hennigan et al.  did not see significant enhancements in the partitioning below 70% RH.
 The ability to observe total OA mass dependence of ΣAN phase partitioning is a unique aspect of this study. This study and that of Hennigan et al.  provide direct evidence (from ambient rather than chamber observations) that absorptive partitioning determines to a significant extent the variability of OA. These observations are challenging to understand in light of recent laboratory studies [e.g., Cappa and Wilson, 2011; Perraud et al., 2012] that have provided evidence that phase partitioning of atmospheric organic compounds, including nitrates, does not follow equilibrium partitioning theory. We suggest that more targeted laboratory and field observations are needed to fully understand the specific differences between the laboratory explorations of specific chemical systems, and field OA observations. To the extent that equilibrium partitioning does control atmospheric OA, the fact that we observe an increase in particle partitioning with total OA while Hennigan et al.  only observed an increase in partitioning with water-soluble OC implies that the activity coefficients of organic compounds in various solvents may play an important and unappreciated role in atmospheric OA formation.
 While the chemical environment in Bakersfield is somewhat unique (high NOx, high NHx, low RH), it is worth noting that daytime nitrate production in the study region was lower than in many other locations with an effective yield near 2.5% for VOC oxidation. Yields double this value are more typical [Perring et al., 2013]. Results from Fry et al.  also point out that the organic nitrates are prominent in aerosol, and we look forward to our own and other research teams making observations in distinctly different environments.
 This work is supported by the California Air Resources Board under grants CARB 08-316 and 09-328. E.C.B. was supported by NASA ESSF fellowship.