UAS Chromatograph for Atmospheric Trace Species (UCATS) – a versatile instrument for trace gas measurements on airborne platforms
- 1Cooperative Institute for Research in Environmental Sciences, University of Colorado Boulder, Boulder, CO 80309, USA
- 2Global Monitoring Laboratory, NOAA, Boulder, CO 80305, USA
- 3Chemical Sciences Laboratory, NOAA, Boulder, CO 80305, USA
- 4John A. Paulson School of Engineering and Applied Sciences, Harvard University, Cambridge, MA 02138, USA
- 5CIMEL Electronique, Paris, 75011, France
- 6Izaña Atmospheric Research Center, Santa Cruz de Tenerife, 38001, Spain
- 7Department of Earth and Environmental Sciences, Columbia University, New York, NY 10027, USA
- 8Lamont-Doherty Earth Observatory, Columbia University, Palisades, NY 10964, USA
- 9Climate and Space Sciences and Engineering, University of Michigan, Ann Arbor, MI 48109, USA
- 10NASA Langley Research Center, Hampton, VA 23681, USA
- 11NASA Ames Research Center, Mountain View, CA 94035, USA
Correspondence: Eric J. Hintsa (firstname.lastname@example.org)
UCATS (the UAS Chromatograph for Atmospheric Trace Species) was designed and built for observations of important atmospheric trace gases from unmanned aircraft systems (UAS) in the upper troposphere and lower stratosphere (UTLS). Initially it measured major chlorofluorocarbons (CFCs) and the stratospheric transport tracers nitrous oxide (N2O) and sulfur hexafluoride (SF6), using gas chromatography with electron capture detection. Compact commercial absorption spectrometers for ozone (O3) and water vapor (H2O) were added to enhance its capabilities on platforms with relatively small payloads. UCATS has since been reconfigured to measure methane (CH4), carbon monoxide (CO), and molecular hydrogen (H2) instead of CFCs and has undergone numerous upgrades to its subsystems. It has served as part of large payloads on stratospheric UAS missions to probe the tropical tropopause region and transport of air into the stratosphere; in piloted aircraft studies of greenhouse gases, transport, and chemistry in the troposphere; and in 2021 is scheduled to return to the study of stratospheric ozone and halogen compounds, one of its original goals. Each deployment brought different challenges, which were largely met or resolved. The design, capabilities, modifications, and some results from UCATS are shown and described here, including changes for future missions.
Accurate and precise measurements of trace gases and other atmospheric parameters have resulted in an ever more detailed understanding of the chemistry and physics of Earth's atmosphere. This has allowed progress on environmental issues of global concern, including stratospheric ozone depletion and air pollution in the lower atmosphere. For example, after the first report of the Antarctic “ozone hole” (Farman et al., 1985), a combination of measurements from balloons, aircraft, and satellites, backed by a wide range of laboratory, theoretical, and modeling studies, allowed a sufficient grasp of the problem to develop an effective international response relatively quickly (Douglass et al., 2014). Though ozone loss and organic halogen emissions are still ongoing matters of concern, climate change driven by greenhouse gas emissions is now the overarching environmental problem today, while air quality continues to be an important issue as well.
The Halocarbons and other Atmospheric Trace Species (HATS) group in what is now the Global Monitoring Laboratory (GML) at the National Oceanic and Atmospheric Administration (NOAA) in Boulder, CO, has long been involved in measuring N2O, CFCs, and other trace gases, primarily by using gas chromatography (GC) with electron capture detectors (ECDs). This led to participation in a series of airborne missions to study halogen budgets, ozone loss, and stratospheric transport, starting on the NASA ER-2 aircraft in 1991 (Elkins et al., 1996). GCs are well suited to measuring multiple trace species in the atmosphere, because with an appropriate column, several compounds can be separated and detected with the same instrument. ECDs are extremely sensitive (a few parts per trillion (ppt) or better) to halogen-containing compounds, including ozone-depleting substances (ODS), and with appropriate modifications can be used to detect other molecules as well. A few other GC instruments have been used for in situ measurements of CFCs (Tyson et al., 1978; Kuster et al., 1981; Vedder et al., 1983; Bujok et al., 2001), and they can now be coupled with mass spectrometric detection (e.g., Apel et al., 2015) as well. With the advent of unmanned aircraft systems (UAS), the potential emerged to extend scientific airborne missions to longer durations and other experiments that were not possible with manned aircraft, as well as eliminate some of the danger of flying piloted aircraft in remote regions. Accordingly, the UAS Chromatograph for Atmospheric Trace Species (UCATS), a smaller and lighter-weight version of previous aircraft instruments, was designed and built to measure ODS and other trace gases on UAS missions. These began in 2005 with the Altair UAS, a high-altitude version of the General Atomics Predator B. Given the limited payload capacity of Altair, small and lightweight ozone and water vapor sensors were installed inside UCATS to generate a more complete data set. After two missions on Altair, UCATS joined the payload of the National Science Foundation/National Center for Atmospheric Research (NSF/NCAR) piloted Gulfstream V (GV) for the START-08 (Stratosphere-Troposphere Analyses of Regional Transport 2008) and HIPPO (HIAPER Pole-to-Pole Observations; 2009–2011) missions (Pan et al., 2010; Wofsy, 2011), which included measurements from near the surface to the lower stratosphere. In 2010, UCATS flew on the NASA Global Hawk UAS for the Global Hawk Pacific (GloPac) demonstration project and participated in the Airborne Tropical Tropopause Experiment (ATTREX; Jensen et al., 2013) from 2011 to 2014, to study dehydration, transport, and ozone chemistry in the tropical tropopause layer (TTL). Most recently, UCATS completed the Atmospheric Tomography Mission (ATom; 2016–2018), for which the NASA DC-8 aircraft sampled the remote atmosphere over the Atlantic, Pacific, and Southern oceans and parts of the Arctic and Antarctic from near the surface to above 12 km in different seasons. Many of these missions required changes to UCATS, and components were also upgraded when possible. The end result is a compact instrument for UAS and piloted aircraft, capable of measurements of atmospheric composition, chemistry, and transport in the stratosphere and troposphere. We describe the design and components of UCATS in Sect. 2, focusing on ATom, the most recent mission for UCATS; improvements and modifications over the course of its missions in Sect. 3; and data and intercomparisons from some of the field campaigns in Sect. 4, with a short summary including future plans in Sect. 5.
At its core, UCATS is similar to previous gas chromatograph (GC) instruments designed and built for aircraft and balloon platforms (Elkins et al., 1996; Romashkin et al., 2001; Moore et al., 2003). It combines a two-channel GC that is a lighter and much more compact version of the four-channel ACATS-IV (Airborne Chromatography for Atmospheric Trace Species IV; Elkins et al., 1996) instrument and incorporates some of the advances in fast chromatography from the LACE (Lightweight Airborne Chromatograph Experiment; Moore et al., 2003) instrument for balloons, along with small ozone and water vapor sensors. Figure 1 shows a block diagram of UCATS with all the major internal components; more detailed drawings of the ozone and water instruments are included in the Appendix (Fig. A1a and b). Each part of UCATS is described in the following subsections.
2.1 Gas chromatographs
Both GC channels use Valco 10- and 12-port two-position valves (VICI, Houston, TX) to control flow switching and ECDs (Valco and Shimadzu) to detect specific trace species with high precision, with added dopant gas as needed (Phillips et al., 1979; Fehsenfeld et al., 1981). In its original configuration, one channel used OV-101 in packed columns to separate and measure CFC-12, halon-1211, and CFC-11 every 70 s, similar to the Lightweight Airborne Chromatograph Experiment (LACE) (Moore et al., 2003). After the initial Altair flights in 2005, these were replaced with Unibeads (pre-column, ∼ 1 m length) and molecular sieve 5A (main column, 0.7 m) to measure molecular hydrogen (H2), methane (CH4), and carbon monoxide (CO) every 140 s. A tiny flow of nitrous oxide (N2O) dopant (∼ 0.003 sccm) added to the ECD is required for adequate sensitivity. Flows and column temperatures varied over different missions; in ATom, with the chromatography optimized for both the troposphere and stratosphere, at a temperature of 94 ∘C the N2 carrier gas flow was 60 sccm, with 4 s of pre-emphasis at 100 sccm at the start of the injection, to rapidly bring the pre-column up to the same pressure as the main column. The pre-column was back-flushed after 25 s to remove any remaining compounds over the remainder of the 140 s time window.
The second channel uses a pre-column (0.6 m) and main column (1.8 m) of Porapak Q, followed by a post-column of 5A molecular sieve (originally 0.20 m, now 0.25 m) to measure sulfur hexafluoride (SF6) and N2O every 70 s; doping the nitrogen carrier gas with CO2 enhances the ECD response to N2O. The pre-columns and main columns were maintained at 91 ∘C and the post-column at ∼ 120 ∘C (for the shorter version) and 190 ∘C (longer version; changed in 2011). Carrier gas flows in ATom were 55 sccm, with the flow in the pre-column reversed after 13–14 s. Since the backflush switches occur early in the cycle, there is sufficient time for the pre-columns in each channel to be cleaned out, even with lower flow rates compared to the main flows. All the columns used were packed in 3.2 mm o.d. stainless-steel tubing, wound around a circular mandrel with heater cartridges and a resistance temperature detector (RTD), and packaged in insulated metal cans. The ECDs were packaged in similar cans but sealed and supplied with a ∼ 5 sccm purge flow to prevent oxidation and maintained at 330 or 350 ∘C with Omega temperature controllers.
Chromatograms are similar to those in Moore et al. (2003), Figs. 7c and 9. ECDs provide very high sensitivity but can have non-linearity, particularly for doped channels, where secondary ion–molecule reactions are used to detect trace species. UCATS was calibrated on the ground during each mission, with a set of standards spanning the range of expected atmospheric concentrations (typically 30 %–100 % of those in background tropospheric air) and occasionally including zero air to check baselines. From these experiments, calibration curves for each molecule are calculated, including an estimate of the error in the calibration. An example of a calibration curve for N2O is included in the Appendix (Fig. A2); all other curves were even closer to linear. In flight, a calibration standard from compressed background tropospheric air is injected every 6–10 min, and the peak heights of air samples and standards are analyzed with the calibration curves to generate a time series of mixing ratios for each molecule in sampled air.
2.2 Airflows and sampling
Ambient air is drawn into UCATS from a side-facing or rear-facing inlet extending 25–30 cm from the skin of the aircraft (outside the aircraft boundary layer) through stainless-steel and Synflex tubing; sample flow tubing inside UCATS is stainless steel. Air is pressurized in the GC sample loops by an external two-stage KNF diaphragm pump (model UN726, with Teflon-coated heads and diaphragms) and maintained at 1225 hPa with an absolute pressure relief valve (Tavco, Inc.; Chatsworth, CA); excess air is dumped through the Tavco overflow. Air flows at approximately 80 sccm sequentially through the two sample loops (∼ 0.5 cc volume for each channel) and a flow meter and is controlled by solenoid valves and a pressure regulator set at 1080 hPa on the outlet. Every 70 or 140 s the contents of the sample loops are injected by the two-position Valco valves onto the pre-columns, providing a discontinuous ∼ 2 s snapshot measurement of ambient air.
2.3 Water vapor
The sample airflow is split just upstream of the GC pump to feed a tunable diode laser (TDL) hygrometer with its own pump (KNF, model NMP850) downstream of the absorption cell. The original hygrometer, a custom commercial sensor from MayComm, Inc., used infrared absorption at 1.37 µm with second harmonic detection to measure water vapor. Since water vapor number densities span 5 orders of magnitude from the surface to the stratosphere, the laser beam was split into two optical paths, a 13.4 cm “short path” for measurements from the surface to the mid-troposphere (40 000 to 500 parts per million (ppm)) and a 403 cm multi-pass “long path” for measurements from the mid-troposphere into the stratosphere (1000 to < 5 ppm). On the Altair missions, with a minimal payload, a small Vaisala probe was installed on the inlet for measurements of temperature, pressure, and relative humidity. This was not used subsequently, as the payloads on larger aircraft included dedicated instruments for meteorological measurements.
During ATom, the TDL hygrometer in UCATS was upgraded with a new model from Port City Instruments (Reno, NV), the successor to MayComm. It is similar in concept and uses a distributed feedback laser (DFB) to scan across two closely spaced absorption lines near 2.574 µm. Absorption at this wavelength is much stronger than in the original instrument, allowing higher sensitivity in the stratosphere. As before, the laser beam is split into two optical paths, with the short path (5.14 cm) for high values of tropospheric water (∼ 2000–40 000 ppm) using direct absorption. The long path (280.0 cm) is used with second harmonic detection for water vapor from 0–100 ppm, and intermediate values (100–5000 ppm) are measured using the long path with direct absorption. A second weak absorption line is also analyzed with direct absorption for water vapor mixing ratios above 1000 ppm; this is not being used at present. Both long- and short-path spectra are recorded simultaneously, with each scan taking approximately 200 ms. All four measurements of water vapor are calculated, and then each one is averaged together for ∼ 1 Hz output on a serial data line. All data are recorded by the UCATS computer, and the appropriate value for display and archiving is chosen based on the range of pressure and water vapor. Both instruments required extensive calibration using prepared water vapor standards and frost point hygrometers for accurate measurements. The new instrument allows higher-precision (±0.1 ppm) measurements of water vapor in the stratosphere compared to the original instrument, which was limited to ±1 ppm.
Ozone was measured by direct absorption (Beer–Lambert law) UV photometers from 2B Technologies (Boulder, CO), modified for high-altitude operation and mounted inside the UCATS package. The initial ozone instrument was a 2B model 205; modifications included a stronger pump (KNF, model UNMP-830), a small metal cylinder upstream of the pump to dampen pressure fluctuations that could degrade the measurement precision, O3 scrubbers with manganese dioxide (MnO2)-coated screens (Thermo Fisher), and pressure sensors with a range from 0 to over 1000 hPa (Honeywell ASDX series). Ambient air was brought to the ozone instruments from the inlet through a separate Teflon tube (6.35 mm o.d.), with the exhaust from the ozone and water instruments combined inside UCATS and released outside the aircraft. The model 205 is a dual-beam photometer, with the flow continuously split between unscrubbed (ambient) air into one cell and scrubbed (ozone-free) air into the other. Two photodiodes located at the end of 15 cm long absorption cells measure the intensity of 254 nm radiation emitted from a mercury lamp. Ozone concentrations are calculated from the ratio of measured intensities through the cells with scrubbed and unscrubbed air according to the Beer–Lambert law. The flow paths are switched by solenoids every 2 s, to allow alternating measurements of ambient and scrubbed air in each cell, with data averaged to 10 s on the original model. The instruments are checked against a NIST-traceable calibration system (Thermo Fisher, model 49i) on the ground before and after every mission. For ATom, a new and more sensitive 2B model 211 ozone photometer was added to UCATS in addition to the original model 205, with similar modifications as before and additional changes as described in Sect. 3.
2.5 Physical characteristics
The overall dimensions of UCATS were initially cm, with a weight of 29 kg. To integrate the new water and ozone instruments for ATom, an additional section was added to the top, increasing the height from 26 to 33 cm and the weight to 33 kg. The external GC pump weighs an additional 5 kg, and fiber-wrapped aluminum bottles (SCI Composites; now Worthington Industries) for compressed nitrogen (N2) carrier gas (model 687) and dry, whole air calibration gas (model 209) for the GC, both filled to ∼ 13 000 kPa, together weigh approximately 7 kg. The total N2 flow (carrier gas, backflush, purge flows) is about 300 sccm. The N2 bottle needed to be filled every one or two flights, the calibration gas was filled once per deployment, and the small dopant bottles could last for over a year without refilling. For flights on passenger aircraft, such as the DC-8 for ATom, the N2 and air bottles can be replaced by larger gas cylinders as weight and space allow. UCATS is powered by 28 V DC, and the complete package draws 12 A at startup (∼ 350 W), decreasing to 150 W after the heaters warm up (∼ 30 min). The majority of the power is consumed by the column and ECD heaters; the GC pump and the TDL use about 1 A each, ozone less than 0.5 A, and other electronics about 1–2 A. Different voltages (+5, ±12, 15, and 24 V) are supplied by Vicor DC–DC converters. The internal wiring in the ECD cans is carefully adjusted to minimize electrical noise on the detector circuits; no other electromagnetic compatibility issues were observed. UCATS is controlled by an Ampro computer with the QNX operating system, and data are stored on flash memory for post-flight processing; quick-look, near-real-time data for ozone, water, N2O, SF6, and CH4 are also provided by a serial or Ethernet connection to the aircraft, for onboard use and telemetry to the ground. Data are analyzed post-flight with home-built software, including GC peak integration and quantitation routines, primarily using Igor software, and three separate data files (GC, ozone, and water, with different time intervals) are generated for archiving and dissemination.
Aircraft missions that included UCATS are summarized in Table 1 and described in this section. The first two projects were designed to show that high-quality measurements could be made on a UAS with autonomous instruments. The NOAA/NASA UAS Demonstration Project using General Atomics' Altair (Predator B-ER) UAS was conducted from Gray Butte, CA, during April–May and November, 2005. UCATS measured N2O, SF6, CFC-11, CFC-12, halon-1211, and ozone. More than 60 h of atmospheric composition data was acquired up to altitudes of 13 km, with the mission highlight an 18.4 h flight over the eastern Pacific Ocean, successfully demonstrating that atmospheric composition and other environmental parameters can be measured with high precision and accuracy from a UAS (Fahey et al., 2006). The NASA/USDA-FS/NOAA Western States Fire Mission was conducted in August and October 2006, again using Altair (Hinkley et al., 2009). The scientific focus was on remote mapping of wildfires from a UAS, with UCATS on board to measure atmospheric trace gases in fire plumes. At this point, the halocarbon GC channel was reconfigured to measure the combustion products CO and CH4, along with H2, and a TDL water vapor sensor was added to UCATS. Accomplishments of this project included 21 and 22 h science flights and more than 65 h of UCATS in situ measurements of trace gases and water vapor.
For START-08 (Pan et al., 2010) and HIPPO (Wofsy, 2011), both UCATS and the PAN and Trace Hydrohalocarbon ExpeRiment (PANTHER), a four-channel GC with ECD detection and a GC with mass spectrometry detection (GC/MS), were flown on the NSF/NCAR GV aircraft. These were integrated together with a NOAA whole air sampler (WAS) in collaboration with the University of Miami (Schauffler et al., 1999). The larger GV payload was designed to probe long-lived greenhouse gases and tracers of atmospheric transport. In HIPPO, the GV flew repeated vertical profiles between 150 m above sea level and 14 km, largely over the Pacific Ocean, from northern Alaska and the Arctic Ocean to south of New Zealand near Antarctica, with five deployments from January 2009 to August 2011 covering different seasons. The first use of UCATS in the extremely humid tropics during HIPPO revealed several issues, which were resolved after the first two deployments. Initially, the GC columns adsorbed water, which changed their retention characteristics. To alleviate this, a Nafion dryer (Perma Pure, MD-050-72S-2) was added to remove most of the moisture from the GC airflow prior to the sample loops, with the exhaust from the pre-columns used as the dry counterflow gas. The Nafion dryer helped considerably, but retention times and sensitivity for the N2O SF6 channel still showed changes after passing through very humid air; likely the Nafion dryer could not remove all the water vapor. As described in Moore et al. (2003), we use Porapak Q columns to separate N2O and SF6 from the large O2 peak. This is followed by a short post-column of 5A molecular sieve, which partially retains the N2O but not SF6, allowing the two peaks to be separated. The molecular sieves have a very high affinity to water vapor, and absorbed water changes the retention characteristics and peak height for N2O. This problem was finally resolved by lengthening the 5A molecular sieve post-column from ∼ 20 to 25 cm. This allowed the post-column to be operated at 190 ∘C instead of 115–120 ∘C, with N2O still completely eluting within 70 s after sample injection. Water does not accumulate in the post-column at the higher temperatures, and retention times and other aspects of the chromatography remained constant. The N2O peak also became much sharper and higher, improving the resolution of SF6 and N2O. This required changes to the electrometer circuit that processes the ECD signal, in order to achieve a faster response time and avoid saturation of the signal. These were completed in 2015, prior to ATom. Plots illustrating data quality and intercomparisons are shown in Sect. 4.
Problems were also identified with the 2B ozone instrument during the START-08 and HIPPO missions related to changing humidity. UV ozone photometers are known to suffer from offsets when transitioning between wet and dry conditions (Wilson and Birks, 2006), because of water being retained in the scrubber and slowly released, differentially affecting reflectance from the walls of the cell with scrubbed air compared to the cell with ambient air. This was resolved for ATom, as described later in this section.
From 2010 to 2014, UCATS was integrated into a compartment in the fuselage of the Global Hawk UAS for the GloPac and ATTREX missions (Jensen et al., 2013). The Global Hawk generally operates in the stratosphere and upper troposphere (12–20 km), where air is very dry. However, these missions led to other changes in order to improve the data quality for ozone. The original 2B model 205 could achieve a precision of ±2 % + 1 part per billion (ppb) with 10 s averaging at atmospheric pressure. Because Beer–Lambert absorption is really a measurement of number density (concentration) of the absorbing molecule, the precision varies inversely with pressure (1 ppb precision at 1000 hPa corresponds to a precision of 10 ppb at 100 hPa, a typical pressure in the upper troposphere and lower stratosphere, UTLS). This is more than adequate for midlatitude and polar stratospheric missions such as GloPac, where ozone varies from a few hundred to a few thousand parts per billion. But for ATTREX, where the focus was the tropical tropopause layer (TTL; Fueglistaler et al., 2009), ozone was typically less than 100 ppb at pressures of 150–70 hPa. To partially address this issue in ATTREX-2 and 3 (2013–2014), a second model 205 sensor was added to UCATS. The original model 205 remained completely enclosed, and the new one was added to the front panel, with part of the instrument inside the sheet metal UCATS enclosure and the cell, lamp, and detectors on the surface, with a small insulated cover and warm airflow from UCATS passing through it. In general, the older 2B had better stability over a flight, possibly because of the more constant temperature environment inside UCATS. However, after a few hours of operation (always the case with Global Hawk flights, which could last for ∼ 24 h with the ATTREX payload), both instruments converged to stable and consistent readings. When both instruments were operating normally, data from the two instruments were merged and averaged to create a combined data set with a value reported every 5 s. By averaging the data to longer times (typically 10 s), the precision of the measurements could be improved. UCATS served as the primary ozone instrument during ATTREX-3, where weight and balance issues with the payload prevented the NOAA CSL instrument from being flown on the Global Hawk.
ATom was similar to HIPPO, but with a much larger payload to map out and study atmospheric chemistry as well as long-lived gases over remote regions. For ATom, a new 2B model 211 ozone photometer was added to UCATS and the partially external model 205 removed. The model 211 is similar in principle but has a longer cell and path length (30 cm compared to 15 cm for the model 205), improved electronics, and built-in flow meters to assure equal flows through each cell, with a stated precision that is the sum of 1 % + 0.5 ppb over a 10 s average at 1000 hPa. As purchased, it used photolysis of N2O to produce NO as the ozone scrubber; this method is not affected by changes in humidity of the sampled air. However, at high altitudes, with fixed addition of N2O (or NO), the rate of the chemical reaction (NO + O3→ NO2+ O2) that removes ozone decreases with decreasing pressure. Rather than trying to add more NO to compensate (carrying toxic gases like NO on an aircraft is problematic; even large amounts of an oxidizer such as N2O add to the complexity of getting a payload certified), we used MnO2-coated screens as the scrubber and passed both the scrubbed and ambient airflows through Nafion moisture exchangers provided with the instrument. Moisture exchangers have been shown to eliminate the artifacts associated with rapid changes in water vapor by keeping both cells at a constant humidity (Wilson and Birks, 2006). They were not used for HIPPO and START-08, because the pressure of the gas flow being analyzed varied from ∼ 100 to 1000 hPa while the cabin pressure is maintained near 900 hPa at high altitudes. With a pressure differential of over 700 hPa, the soft Nafion tubes could leak or collapse and block the flow. We solved this potential problem in ATom by placing the Nafion tubes in a small aluminum box (McMaster-Carr, 75895K series), sealed to the outside except for a small flow (50–200 sccm) of moist air (cabin air passed through a short piece of 12.7 mm o.d. tube containing wet cotton) through the box and into the exhaust line from the ozone instrument. Thus, the pressure inside and outside the Nafion tubes stayed approximately equal. This setup adds moisture to dry air samples, and may actually remove some water from the very wettest samples (such as the tropical marine boundary layer, where the water content can exceed 3 %), and generally keeps the humidity in the ozone instrument constant or at least the same in both the scrubbed and unscrubbed flows. This simple solution eliminated the effects of rapid changes in humidity, as demonstrated by comparisons with another ozone instrument (see Figs. 9 and 10 below).
The new ozone and water instruments were larger than the original models and could not fit into the existing UCATS shell. A 7.5 cm extension was added to the top of UCATS, with the new water and ozone instruments and main cooling fans secured to the top plate. The original 2B model 205 ozone instrument was left on the side to enable a comparison of results and to provide a known and reproducible pressure measurement when needed. The total weight increase was about 5 kg, but this is negligible on an aircraft with the size and capacity of the DC-8. Starting in 2019, an additional repackaging and upgrade of UCATS has been carried out for flights on the ER-2 aircraft; this is described in Sect. 5.
In this section, we present results in the stratosphere first and then in the troposphere. To compare with UCATS, we used data from several other instruments. On the GV, the quantum cascade laser spectrometer (QCLS; Santoni et al., 2014) measured long-lived trace gases, including N2O and CH4, with high precision and 1 s time resolution, ideal for comparing time series and tracer–tracer correlation plots. The PANTHER instrument (a four-channel GC, with a separate GC/mass spectrometer) also measured the same molecules by GC as UCATS, using similar techniques. Whole air samples were collected in glass flasks using programmable flask package units (PFPs), which could be filled on demand or in a preset sequence, with 24 samples typically collected per flight. Samples were later analyzed at the NOAA Global Monitoring Laboratory for a large set of trace gases (Sweeney et al., 2015). All these instruments were also on the DC-8 aircraft for ATom. Data from the Airborne Chromatograph for Atmospheric Trace Species (ACATS; Elkins et al., 1996), a predecessor of both PANTHER and UCATS, are also used from the 1997 Photochemistry of Ozone Loss in the Arctic Region in Summer (POLARIS) mission for reference.
The NOAA Chemical Sciences Laboratory (CSL) classic ozone instrument (Proffitt and McLaughlin, 1983) has a long history of measurements on high-altitude aircraft and flew on the GV during HIPPO. This was replaced with a new lighter version, NOAA-2 (Gao et al., 2012), for Global Hawk missions. A different group from NOAA CSL flew a chemiluminescence (CL) instrument on the DC-8 in ATom for measurements of ozone (Bourgeois et al., 2020), NO, NO2, and total reactive nitrogen (NOy). Ozone data from concurrent GML sonde launches (Komhyr et al., 1995) and the NCAR chemiluminescence instrument (Ridley et al., 1992), on the GV during the Convective Transport of Active Species in the Tropics (CONTRAST) mission, were also used for ATTREX data comparisons and analysis.
The diode laser hygrometer (DLH; Diskin et al., 2002; Podolske et al., 2003), an open-path near-infrared absorption instrument, whose optical path is defined by a transceiver in the fuselage and a retroreflector mounted below one of the wings, was used to measure water vapor on the Global Hawk and DC-8. During ATTREX, the NOAA CSL TDL hygrometer (also from Port City Instruments) measured water vapor as well. The Meteorological Measurement System (MMS; Scott et al., 1990) was used on the Global Hawk and DC-8 missions for position and meteorological variables.
4.1 Gas chromatographs
Global Hawk flights during the GloPac mission covered a wide range of air masses in the stratosphere and provided an opportunity to demonstrate the capabilities of UCATS in the environment for which it was designed. Figure 2 shows a scatter plot of SF6 vs. N2O mole fractions for the flight of 23 April 2010 from Edwards Air Force Base, CA, to the western Arctic Ocean and back (∼ 35–85∘ N, 120–165∘ W) at altitudes from 16 to 20 km, with two profiles down to 13 km and back. N2O and SF6 are long-lived greenhouse gases emitted at Earth's surface and generally decline with altitude in the stratosphere (e.g., Plumb and Ko, 1992). For N2O this is primarily due to photochemical loss in the stratosphere, and for SF6 it is because older air entered the stratosphere at earlier times, when tropospheric SF6 mixing ratios were lower (Hall et al., 2011). As a result, N2O and SF6 are correlated in the stratosphere, with older air and air from higher altitudes having the lowest mixing ratios for both gases. This correlation can be seen in Fig. 2, where N2O declines strongly from its tropospheric value (∼ 320 ppb in 2010) as SF6 (tropospheric value ∼ 7 ppt in 2010) approaches 5.5 ppt. Data from ACATS-IV taken on the ER-2 aircraft almost 13 years earlier in the Arctic during the 1997 POLARIS mission are shown with the GloPac data for reference. POLARIS N2O and SF6 mixing ratios were adjusted upward for the tropospheric growth over the 13 years between missions (N2O increased from 312.5 to 322.9 ppb and SF6 from 3.9 to 7.0 ppt) by adding the difference in SF6 tropospheric values to the POLARIS data and multiplying the ratio of tropospheric values to the POLARIS data for N2O and other tracers that are photochemically destroyed in the stratosphere. This is mainly to bring the two data sets onto the same scale for easy visualization, though the similarity does reflect the relatively stable nature of stratospheric circulation and photochemistry. Average tropospheric values of these long-lived greenhouse gases were taken from the NOAA GML network (http://www.esrl.noaa.gov/gmd/ccgg/trends/global.html, last access: 29 September 2021). The measurement precision for UCATS is about ±0.05 ppt SF6 (1σ) and ±1.5 ppb N2O, similar to ACATS but with a data rate of every 70 s instead of 360 s. The slightly more gradual slope for POLARIS data is due to the fact that SF6 was increasing more slowly in the 1990s than in the years just before GloPac (Hall et al., 2011) and perhaps other more subtle differences in the trends. Similar plots of GloPac and (adjusted) POLARIS CH4 vs. N2O and H2 vs. CH4 data from the same flights (Fig. 3) show close correspondence between the two campaigns and tight, nearly linear correlations, as expected from the fact that these are all long-lived gases in the stratosphere. Overall, UCATS precision for CH4 and H2 was ±7–8 ppb (0.5 %) and ±5 ppb (1 %) respectively, equal to or slightly better than that of ACATS-IV and with a slightly faster data rate.
The START-08 and HIPPO missions were the first tropospheric campaigns for UCATS. On 12 January 2009, during the first HIPPO deployment, the GV sampled air in both the troposphere and stratosphere as it traveled from Anchorage, AK, north to near 80∘ N over the Arctic Ocean and back. The precision for UCATS N2O during most of the flight was near ±1 ppb in both the troposphere and stratosphere, calculated from flight segments with near-constant N2O near the start of the flight and comparisons with QCLS and PFP samples throughout the flight (Fig. 4a). A more quantitative comparison can be made by plotting UCATS and PFP data for the entire HIPPO 1 deployment against the higher-time-resolution QCLS data (Fig. 4b). Each UCATS GC measurement is a roughly 2 s average of the atmospheric composition along the flight path a few seconds before the air sample is injected and is plotted here against the corresponding 10 s average of QCLS data. Each PFP flask takes between 30 s and a few minutes to fill, depending on altitude, and a comparison with QCLS data is enabled by averaging the QCLS data over the sampling interval associated with each flask sample. QCLS data have been corrected here for the approximately 1 ppb offset with respect to the PFPs reported by Santoni et al. (2014) during HIPPO in 2009–2011. The UCATS vs. QCLS correlation allows an upper limit estimate of UCATS precision, assuming all the error is associated with the UCATS measurements, none from QCLS, and that effects related to atmospheric variability arising from timing mismatches are negligible. The resulting standard deviation (1σ precision) is ±1–2 ppb over the entire month of HIPPO flights, from the high Arctic through the tropics to the Southern Ocean and back. The slope of the fit is 0.91 ± 0.004; this difference has not been resolved. We note that the slope for the PFP data is 0.93 ± 0.02, though this is partially driven by the smaller slope for tropospheric (high N2O) data, as opposed to for UCATS, where the slope is also smaller in the troposphere but clearly reflects differences in the stratosphere (low N2O), where the dynamic range of N2O is large. The UCATS and PFP results agree closely over the more limited range of PFP N2O data, but because the measurements were not simultaneous, a quantitative comparison is not possible.
In ATom, with the GC system optimized for all conditions, UCATS produced precise and accurate data in the troposphere with both short- and long-term stability and without degradation in the humid tropics. This is demonstrated by N2O and SF6 time series for the DC-8 flight of 29 January 2017, from Palmdale, CA, to northern Alaska and back to Anchorage (∼ 35–70∘ N, 120–155∘ W), and scatter plots for the entire ATom-2 deployment (Fig. 5). Data from UCATS, PANTHER, QCLS (N2O only), and PFPs show excellent agreement for the time series (mean differences typically ±1–2 ppb N2O and ±0.05 ppt SF6). ATom QCLS N2O data show a similar offset relative to PFPs (taken as the reference instrument on board) as observed during HIPPO, attributed to the QCLS calibration procedure. As in Gonzalez et al. (2021), QCLS N2O data are corrected by subtracting the offset with respect to the PFP data (∼ 1.2 ppb). The 1σ precision of UCATS and PANTHER was ∼ ±1 ppb N2O and ±0.05 ppt SF6 from both the time series and the scatter plots (again assuming all the variability in the comparison with QCLS is associated with the GC data). As described above, SF6 and N2O are well correlated in the stratosphere, and the precision of SF6 from the lower right panel can be estimated for stratospheric data (lower values of both gases). In the troposphere, the plot reflects the strong latitudinal gradient in SF6, with lower SF6 in the Southern Hemisphere and higher SF6 in the Northern Hemisphere. This leads to a much steeper apparent slope, since N2O also has a latitudinal gradient, but weaker, also with lower values in the Southern Hemisphere. Transitions between the troposphere and the stratosphere lead to mixing lines between the two branches (from ∼ 310–330 ppb N2O). The only disagreement for N2O is at low values, where PANTHER and UCATS both measure about 3 ppb lower than the QCLS instrument, a deviation in the opposite direction compared to HIPPO. The tropical flight of 3 February 2017 (Fig. A3) illustrates the precision of N2O and SF6 where air masses sampled along the flight track varied slowly (because of its altitude range, the DC-8 is always in the troposphere at these latitudes). H2 measurements also showed good agreement between UCATS, PANTHER, and PFPs (Fig. 6), with nearby data points from the different instruments typically differing by about ±5 ppb (1 %) over the entire range of observed values. Values for precision and agreement of measurements from ATom and other missions are summarized in Table 2.
a For these measurements, UCATS agreed to 1–2 ppb with PFP whole air samples; we consider these to be the most precise and accurate measurements of N2O. Agreement with QCLS in the troposphere was also 1–2 ppb but diverged for N2O < 300 ppb, with differences up to 4 ppb. The goal of HIPPO was to quantify long-lived tracers and other greenhouse gases in the troposphere, with less emphasis on the stratosphere. Because UCATS is calibrated with a range of standards from 160–322 ppb in HIPPO, we are confident in our measurements throughout the stratosphere, though these calibrations are performed on the ground and only one standard (with mixing ratios close to the background troposphere) is used in flight. b Precision for water vapor is best expressed as a percentage in the troposphere (high water vapor) and an absolute number in the stratosphere (low water). The precision here is given for the lowest water vapor values in the stratosphere, 1 ppm for the original MayComm instrument and 0.1 ppm for the newer Port City instrument. The precision in the troposphere was always 5 % or better. Calibration and comparison of the Port City instrument are still ongoing. c The precision and agreement for ozone are best expressed in parts per billion at low mixing ratios and as a percentage at high mixing ratios. For example, in ATTREX and GloPac, where ozone ranged from less than 20 to over 2000 ppb, the average agreement with the CSL instrument was better than 1 ppb for ozone < 200 ppb, with a precision better than 10 ppb, and for ozone > 500 ppb, the average agreement was better than 1 %, with a precision of 2 %–3 %. Values for ATom are for tropospheric data (O3<100 ppb), since the focus of ATom was on tropospheric chemistry.
4.2 Ozone – stratosphere
This section is primarily focused on the ATTREX mission, which was designed to probe the chemical composition of air over the tropical Pacific and transport into the stratosphere but applies to all UCATS stratospheric data. Because ozone mixing ratios peak in the stratosphere, the main requirements for a stratospheric ozone measurement are accuracy and stability, with sensitivity to low values usually less critical. In GloPac, the 2B model 205 in UCATS agreed within 1 % with the NOAA classic ozone instrument over the large observed range of ozone mixing ratios (Fig. A4). However, as discussed in Sect. 3, requirements are different in the TTL, where ozone mixing ratios are very low, often less than 30 ppb. Both measurement accuracy and precision are essential at these low values, and even errors of a few parts per billion in ozone (or small measurement biases in water vapor and other trace gases) can lead to different interpretations of the underlying atmospheric processes. The accuracy of the model 205 ozone instrument can be calculated similarly to Proffitt and McLaughlin (1983), where the most important uncertainties are the absorption cross section of ozone, the accuracy of cell temperature and pressure measurements, the absorption path length, and any nonlinearities in detector response. These add up to a few percent, but the initial calibration of the 2B instruments against a reference standard (by 2B) should correct for any slight inaccuracies. In all our calibration checks, the slope was within 1 % of unity and the offset less than 2 ppb (usually < 1 ppb) at ambient pressure (∼ 840 mbar in Boulder, CO, and 920 mbar in California) and room temperature.
As described in Sect. 3, two model 205 sensors were flown in UCATS during ATTREX-2 and 3, with data from the two instruments merged into a single data set with faster time resolution than the original instrument. A comparison of UCATS and NOAA-2 ozone data from ATTREX-2 (Fig. 7) shows that the slope is close to unity with a crossover point near 500 ppb. At low ozone (20–30 ppb), the UCATS data are on average lower by 3–4 ppb. Since the absorption cross sections are the same for both instruments and cell length is fixed (and measured to better than 1 % accuracy), the principal known sources of error are inaccuracies in measured cell temperature and pressure. The pressure sensor in the older 2B instrument was carefully calibrated over a range of pressures for many years (2010–2016) and was stable throughout that time. A small correction was made to account for the pressure drop from the cell to its outlet (where pressure is measured). This introduced about a 1 % increase in ozone at the highest altitudes but was negligible at lower altitudes. Temperature is measured on the cell body rather than in the airflow, but air temperature should have time to equilibrate inside UCATS before reaching the ozone instruments. (Flow to each 2B is ∼ 10 % of that for NOAA-2, which has been shown to measure temperature accurately after warming ambient air as it flows to the cell (Gao et al., 2012).) The offset between NOAA-2 and 2B data bears further examination. UV ozone photometers have been shown to produce offsets when transitioning from wet to dry conditions (Wilson and Birks, 2006), and that is certainly the case for the model 205, as discussed in the following section. However, except on initial ascent, air sampled in ATTREX was always extremely dry, and any artifact should become negligible within 1 h. Similar agreement between NOAA-2 and the original 2B instrument was obtained on ATTREX-1 and GloPac. Laboratory tests for measurement artifacts of the 2B under various conditions produced mostly negligible offsets and always less than 5 ppb.
During ATTREX-3, payload weight and balance issues prevented the NOAA-2 instrument from being flown on the Global Hawk. Coincident balloon-borne electrochemical concentration cell (ECC) ozonesonde launches from Guam provide a comparison for these flights. Data from the last 2 h of the 16–17 February 2014 Global Hawk flight (Fig. 8) most closely overlapped one of the balloon profiles in space and time (within 100 km and 1–2 h). The agreement between the ECC and the 2B instruments in the troposphere (< 16 km, where the balloon and aircraft were in closest proximity) is quite good and shows no significant bias in the UCATS data. A further check on UCATS ozone data is shown in Fig. A5 with ozone data from the GV aircraft (operating during the concurrent CONTRAST mission; Pan et al., 2017), the Global Hawk, and the Guam ozonesonde launch, which was timed to overlap with the return of the Global Hawk on 13 February. In summary, based on laboratory calibrations, tests, and in-flight comparisons, we assign a systematic uncertainty of less than 5 ppb to our model 205 ozone data in the TTL and lower stratosphere. The precision in the TTL ranged from ±5 to 10 ppb but can be improved by temporal averaging. The low values of ozone in the TTL demonstrate the importance of precise and sensitive ozone measurements in this region and the need to minimize or eliminate any systematic errors.
4.3 Ozone – troposphere
As described above, the model 205 in UCATS disagreed with the NOAA classic ozone instrument during HIPPO following transitions between wet and dry air. Most flights had only minor artifacts, but the issue was most pronounced in the tropics, with an example shown in Fig. 9 (top). At low altitudes there was generally good agreement (mean difference is 0.4 ppb, standard deviation is ±4.2 ppb for HIPPO 4), but as the GV aircraft climbed out of the very wet lower troposphere to higher altitudes, or descended back into the lower troposphere, changes in water retained in the scrubber likely affected the reflected light along the sides of the cell, causing anomalous ozone readings. Even though flows were greater than 1 L/min, the instrument took 15 min or more to recover. In ATom, with the newer model 211 instrument and moisture exchangers for both scrubbed and unscrubbed air, the agreement was much closer over a similar flight track, and there were no anomalous data segments as the DC-8 ascended and descended (Fig. 9, bottom). The one discrepancy is in the tropical marine boundary layer (MBL), where UCATS was typically a few parts per billion higher than the chemiluminescence instrument. This disagreement is outside the combined uncertainties of the two instruments and is not currently understood; UCATS showed no differences when calibrated with wet or dry air in the laboratory, and the effect of water vapor on the chemiluminescence instrument has recently been re-checked. There were no offsets in the high-latitude MBL (agreement within 1 ppb; see Fig. A7), so it is presumably related to the high humidity or something else present in the tropical MBL.
Scatter plots of UCATS ozone data against the corresponding instrument from NOAA CSL (Fig. 10) showed reasonable overall agreement in HIPPO, with the slope within 1 % of unity. But in HIPPO, there are many UCATS data points in the troposphere with significantly higher ozone than measured by the NOAA classic ozone instrument (e.g., near 50 ppb). The improvement between HIPPO (top) and ATom (bottom) is dramatic. This is partly due to the longer optical path length in the model 211, as well as other instrumental improvements, but the addition of the Nafion moisture exchangers makes a substantial difference as the aircraft transitions between wet and dry air masses. It should be noted that the NOAA CSL instruments being compared to here have completely different designs – the classic ozone instrument is a UV photometer like the 2B, while in ATom, ozone was detected by chemiluminescence, though it is fundamentally calibrated using an optical measurement. Both of these instruments have a precision in the troposphere of about ±0.5 ppb. The larger deviations occasionally observed in the ATom data are mostly due to timing mismatches during flight segments with sharp gradients in ozone, along with occasional outliers from all instruments (see Fig. A6). The older model 205 was also flown during ATom as a backup and for comparison with the model 211; the model 205 showed some of the same deviations between wet and dry air as in HIPPO, while the model 211 with Nafion moisture exchangers tracked the CSL instrument closely. For many applications, such as climatologies, chemical modeling, and transport studies in the troposphere, the precision of the model 211 (±0.5 ppb at sea level) as flown during ATom is more than adequate, given the good overall agreement with the chemiluminescence instrument. In the stratospheric parts of the ATom flights, the model 211 instrument had precision of about ±1 % and agreement within 2 % (not shown).
4.4 Water vapor
The original MayComm TDL instrument was used in UCATS from 2006 to the first ATom deployment in July–August 2016. Its uncertainty was the sum of 5 % + 1 ppm, based on laboratory calibrations with gravimetrically prepared standards and frost point hygrometers. The ±1 ppm precision limit made stratospheric measurements above ∼ 16 km (where water vapor is typically 2–8 ppm) somewhat qualitative compared to the troposphere and lower stratosphere (H2O > 10 ppm). In addition, there was a temperature effect on the electronics of the long-path channel (for low water vapor) such that the sensitivity dropped with increasing temperature inside UCATS, up to 30 % in extreme cases. This was addressed by adding a Peltier cooling circuit to the TDL electronics box during HIPPO, which kept it at 25 ∘C (except on occasional cold or very warm takeoffs), and also by calibrating and correcting for the temperature effect.
For ATom (starting with deployment 2, January–February 2017), we integrated a new, larger TDL instrument from Port City Instruments, the successor to MayComm. The longer wavelength (2.574 µm vs. 1.37 µm) utilizes stronger absorption lines for a precision of ±0.1 ppm or better in the stratosphere; it can also measure up to 40 000 ppm water vapor, higher than the maximum in the tropical MBL. Similar to the previous instrument, the large dynamic range was achieved by using two optical paths in the cell, strong and weak absorption lines, and different measurement techniques as described in Sect. 2.3. The data were found to have minimal or at least much less sensitivity to instrument temperature compared to the earlier version. For calibrations up to 200 ppm, we used ultra-pure air and gravimetrically prepared standards (Brewer et al., 2020). We also calibrated the instrument over the full range of water vapor mixing ratios and pressures found in the troposphere and lower stratosphere (near 0 to ∼ 30 000 ppm and ∼ 100–1000 mbar) with a bubbler and a frost point hygrometer (MBW, model 373LX). Air from the bubbler (or the standards) was passed through the TDL cell and then to the MBW, as well as to both instruments in parallel. Illustrative plots and in-flight comparisons for both instruments are shown in Fig. 11. Calibrations of the TDL are ongoing, as disagreements with the DLH instrument were observed in ATom, particularly at very high water vapor mixing ratios, > 20 000 ppm, where the TDL data seem to be anomalously high (not shown).
The UCATS instrument integrates three different sensor systems into one compact package for use on UAS and piloted aircraft. The combination of ozone, water vapor, and long-lived trace gases allows for stand-alone experiments with few if any other instruments. It can also contribute to missions on large platforms by measuring selected (and different) long-lived tracers by GC/ECD and also by providing backup measurements of species such as ozone and water. UCATS relied on technology developed for the ACATS instrument (Elkins et al., 1996) and improvements to chromatography for the LACE balloon instrument (Moore et al., 2003). Further improvements made for UCATS were largely to mitigate the effects of water vapor on the GC and ozone systems, allowing measurements throughout the troposphere and stratosphere, as well as continued upgrades of all components.
Over a decade and a half, UCATS has successfully provided trace gas measurements on different types of aircraft for atmospheric science missions with diverse sets of objectives. After demonstration projects focused on the stratosphere, it was used for studies of stratosphere–troposphere exchange and atmospheric transport (START-08 and HIPPO), entry of air into the tropical stratosphere and TTL composition (ATTREX), and tropospheric chemistry (ATom). Over the course of these projects, UCATS evolved from a stratospheric instrument for small UAS payloads to an important contributor on multi-instrument campaigns and geographically extensive tropospheric missions. Table 2 summarizes the data quality over several missions, reflecting improvements in stability for measurements of N2O and SF6, as well as improvements in precision and accuracy for ozone. Data from UCATS have been used to help constrain the interhemispheric difference in OH radical concentrations (Patra et al., 2014) and quantify tropospheric age of air and transport using SF6 (Waugh et al., 2013). Studies have also been performed with UCATS data to probe the composition and structure of the TTL, including halogen chemistry (Jensen et al., 2017; Werner et al., 2017; Navarro et al., 2017), and hydroxyl radical reactivity in the remote troposphere (Thames et al., 2020). At present, UCATS continues to evolve and has now been upgraded and repackaged for the NASA Dynamics and Chemistry of the Summer Stratosphere (DCOTSS) mission. The initial impetus for this change came from the fact that the UCATS enclosure, extended to accommodate the new ozone and water instruments for ATom, no longer fits in the vertical space available in the upper Q-bay of the ER-2 aircraft, which will be used for DCOTSS. Since the focus of DCOTSS is on stratospheric ozone and halogen chemistry, the GC is configured to measure N2O, SF6, and CFCs (as initially flown on Altair in 2005), and a third GC channel has been added to measure shorter-lived chlorocarbons including chloroform (CHCl3), carbon tetrachloride (CCl4), and trichloroethylene (C2HCl3). These changes will allow us to measure much of the organic chlorine budget, including the major long-lived organic chlorine compounds and a few of the more short-lived ones. The repackaged UCATS also has a cleaner and more rational layout, with modular and removable GC channels, ozone, and water instruments, as well as more modern electronics, flow controllers, and pressure controllers. Test and science flights on the NASA ER-2 aircraft are now underway in 2021.
Further details about the UCATS instrument and results from different campaigns are collected here. They include schematics of the ozone and water components, additional data and comparison figures, and details about precision and agreement with other measurements.
A1 Ozone and water instrument schematics
A2 GC calibrations
A3 Tropical N2O and SF6 data
A4 GloPac ozone
A5 ATTREX ozone consistency between different platforms
HIPPO data are publicly available at https://www.eol.ucar.edu/field_projects/hippo (last access: 18 October 2021) and at https://doi.org/10.26023/P1G0-ZSMS-240B (Wofsy et al., 2011) and https://doi.org/10.26023/HSPN-PGNV-WA0M (Hurst et al., 2011). GloPac, ATTREX, and POLARIS data are available at https://espoarchive.nasa.gov/archive/browse/glopac (Hintsa et al., 2010), https://espoarchive.nasa.gov/archive/browse/attrex (Hintsa et al., 2014), and https://espoarchive.nasa.gov/archive/browse/polaris (Elkins et al., 1998), respectively. ATom data are available at http://espoarchive.nasa.gov/archive/browse/atom (last access: 18 October 2021), https://daac.ornl.gov/ATOM/campaign/ (last access: 18 October 2021), and at https://doi.org/10.3334/ORNLDAAC/1581 (Wofsy et al., 2018).
EJH maintained and operated the UCATS instrument since May 2009, analyzed the data presented here, and wrote the manuscript; FLM designed and built UCATS, operated it on several missions, and worked closely with it throughout; DFH operated UCATS on its first UAS missions and helped to prepare this paper; GS Dutton, BDH, JDN, SAM, LPW, AM, and JWE assisted with laboratory work and field missions; JWE was the principal investigator for UCATS for all NASA and NOAA missions through 2020; BRM, SAM, EGH, AFJ, AWR, TDT, LAW, CRT, JP, IB, TBR, BCD, YGR, RC, JVP, SCW, EK, GS Diskin, and TPB provided data and helped with other aspects of the field missions. All the coauthors provided extensive comments and information for this paper.
The authors declare that they have no conflict of interest.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
This work would not have been possible without the pilots, crew, and staff of the various aircraft involved, the NCAR Research Aviation Facility, and the NASA Earth Science Project Office. We are grateful to Ru-Shan Gao for discussions, technical expertise, and other support. We thank Andrew Weinheimer, Denise Montzka, and Lisa Kaser for ozone data from the GV during ATTREX and CONTRAST, Craig Williford and Andrew Turnipseed for help with 2B ozone instruments, Randy May for many helpful discussions about TDL water instruments, and Mathew Gentry for thoughtful comments on this paper.
Support was provided for HIPPO by NSF award no. AGS-0628452, for ATTREX by NASA Earth Venture program award no. NNA11AA55I, and for ATom by NASA award no. NNH17AE26I; additional support was provided by NASA Upper Atmosphere Research Program award no. NNH13AV69I. This work was also supported in part by the NOAA Cooperative Agreement with CIRES, NA17OAR4320101. James W. Elkins, Bradley D. Hall, and Stephen A. Montzka were supported by NOAA’s Climate Program Office (CPO).
This paper was edited by Thomas Röckmann and reviewed by Marc von Hobe and one anonymous referee.
Anderson, D., Nicely, J., Salawitch, R., Canty, T. P., Dickerson, R. R., Hanisco, T. F., Wolfe, G. M., Apel, E. C., Atlas, E., Bannan, T., Bauguitte, S., Blake, N. J., Bresch, J. F., Campos, T. L., Carpenter, L. J., Cohen, M. D., Evans, M., Fernandez, R. P., Kahn, B. H., Kinnison, D. E., Hall, S. R., Harris, N. R. P., Hornbrook, R. S., Lamarque, J.-F., Le Breton, M., Lee, J. D., Percival, C., Pfister, L., Pierce, R. B., Riemer, D. D., Saiz-Lopez, A., Stunder, B. J. B., Thompson, A. M., Ullmann, K., Vaughan, A., and Weinheimer, A. J.: A pervasive role for biomass burning in tropical high ozone/low water structures, Nat. Commun. 7, 10267, https://doi.org/10.1038/ncomms10267, 2016.
Apel, E. C., Hornbrook, R. S., Hills, A. J., Blake, N. J., Barth, M. C., Weinheimer, A., Cantrell, C., Rutledge, S. A., Basarab, B., Crawford, J., Diskin, G., Homeyer, C. R., Campos, T., Flocke, F., Fried, A., Blake, D. R., Brune, W., Pollack, I., Peischl, J., Ryerson, T., Wennberg, P. O., Crounse, J. D., Wisthaler, A., Mikoviny, T., Huey, G., Heikes, B., O'Sullivan, D., and Riemer, D. D.: Upper tropospheric ozone production from lightning NOx-impacted convection: Smoke ingestion case study from the DC3 campaign, J. Geophys. Res., 120, 2505–2523, https://doi.org/10.1002/2014JD022121, 2015.
Bourgeois, I., Peischl, J., Thompson, C. R., Aikin, K. C., Campos, T., Clark, H., Commane, R., Daube, B., Diskin, G. W., Elkins, J. W., Gao, R.-S., Gaudel, A., Hintsa, E. J., Johnson, B. J., Kivi, R., McKain, K., Moore, F. L., Parrish, D. D., Querel, R., Ray, E., Sánchez, R., Sweeney, C., Tarasick, D. W., Thompson, A. M., Thouret, V., Witte, J. C., Wofsy, S. C., and Ryerson, T. B.: Global-scale distribution of ozone in the remote troposphere from the ATom and HIPPO airborne field missions, Atmos. Chem. Phys., 20, 10611–10635, https://doi.org/10.5194/acp-20-10611-2020, 2020.
Brewer, P. J., Gieseking, B., Ferracci, V. F., Ward, M., Carroll, P., Bell, S., and Hall, B.: International pilot study CCQM-P193: 10µmol/mol water vapour in nitrogen, Metrologia, 57, 08015, https://doi.org/10.1088/0026-1394/57/1A/08015, 2020.
Bujok, O., Tan, V., Klein, E., Nopper, R., Bauer, R., Engel, A., Gerhards, M., Afchine, A., McKenna, D. S., Schmidt, U., Wienhold, F. G., and Fischer, H.: GHOST – A Novel Airborne Gas Chromatograph for In Situ Measurements of Long-Lived Tracers in the Lower Stratosphere: Method and Applications, J. Atmos. Chem., 39, 37–64, 2001.
Diskin, G. S., Podolske, J. R., Sachse, G. W., and Slate, T. A.: Open-path airborne tunable diode laser hygrometer, Diode Lasers and Applications in Atmospheric Sensing, International Society for Optics and Photonics, Proc. SPIE 4817, https://doi.org/10.1117/12.453736, 2002.
Douglass, A. R., Newman, P. A., and Solomon, S.: The Antarctic ozone hole: An update, Phys. Today, 67, 42–48, https://doi.org/10.1063/PT.3.2449, 2014.
Elkins, J. W., Fahey, D. W., Gilligan, J. M., Dutton, G. S., Baring, T. J., Volk, C. M., Dunn, R. E., Myers, R. C., Montzka, S. A., Wamsley, P. R., Hayden, A. H., Butler, J. H., Thompson, T. M., Swanson, T. H., Dlugokencky, E. J., Novelli, P. C., Hurst, D. F., Lobert, J. M., Ciciora, S. J., McLaughlin, R. J., Thompson, T. L., Winkler, R. H., Fraser, P. J., Steele, L. P., and Lucarelli, M. P.: Airborne gas chromatograph for in situ measurements of long-lived species in the upper troposphere and lower stratosphere, Geophys. Res. Lett., 23, 347–350, https://doi.org/10.1029/96GL00244, 1996.
Elkins, J., Wamsley, P., Hurst, D., Romashkin, P., and Dutton, G.: POLARIS ACATS IV data [data set], available at: https://espoarchive.nasa.gov/archive/browse/polaris (last access: 14 October 2021), 1998.
Fahey, D. W., Churnside, J. H., Elkins, J. W., Gasiewski, A. J., Rosenlof, K. H., Summers, S., Aslaksen, M., Jacobs, T. A., Sellars, J. D., Jennison, C. D., Freudinger, L. C., and Cooper, M.: Altair unmanned aircraft system achieves demonstration goals, EOS Trans. AGU, 87, 197, 201, available at: https://uas.noaa.gov/Portals/5/Docs/Library/Fahey_Altair_EOS_16May.pdf (last access: 30 September 2021), 16 May 2006.
Farman, J. C., Gardiner, B. G., and Shanklin, J. D.: Large losses of total ozone in Antarctica reveal seasonal ClOx/NOx interaction, Nature, 315, 207–210, https://doi.org/10.1038/315207a0, 1985.
Fehsenfeld, F. C., Goldan, P. D., Phillips, M. P., and Sievers, R. E.: Selective electron-capture sensitization, in: Electron capture: theory and practice in chromatography, edited by: Zlatkis, A. and Poole, C. F., J. Chromatography Library, Elsevier, 20, 69–90, 1981.
Fueglistaler, S., Dessler, A. E., Dunkerton, T. J., Folkins, I., Fu, Q., and Mote, P. W.: Tropical Tropopause Layer, Rev. Geophys., 47, RG1004, https://doi.org/10.1029/2008RG000267, 2009.
Gao, R. S., Ballard, J., Watts, L. A., Thornberry, T. D., Ciciora, S. J., McLaughlin, R. J., and Fahey, D. W.: A compact, fast UV photometer for measurement of ozone from research aircraft, Atmos. Meas. Tech., 5, 2201–2210, https://doi.org/10.5194/amt-5-2201-2012, 2012.
Gonzalez, Y., Commane, R., Manninen, E., Daube, B. C., Schiferl, L. D., McManus, J. B., McKain, K., Hintsa, E. J., Elkins, J. W., Montzka, S. A., Sweeney, C., Moore, F., Jimenez, J. L., Campuzano Jost, P., Ryerson, T. B., Bourgeois, I., Peischl, J., Thompson, C. R., Ray, E., Wennberg, P. O., Crounse, J., Kim, M., Allen, H. M., Newman, P. A., Stephens, B. B., Apel, E. C., Hornbrook, R. S., Nault, B. A., Morgan, E., and Wofsy, S. C.: Impact of stratospheric air and surface emissions on tropospheric nitrous oxide during ATom, Atmos. Chem. Phys., 21, 11113–11132, https://doi.org/10.5194/acp-21-11113-2021, 2021.
Hall, B. D., Dutton, G. S., Mondeel, D. J., Nance, J. D., Rigby, M., Butler, J. H., Moore, F. L., Hurst, D. F., and Elkins, J. W.: Improving measurements of SF6 for the study of atmospheric transport and emissions, Atmos. Meas. Tech., 4, 2441–2451, https://doi.org/10.5194/amt-4-2441-2011, 2011.
Hinkley, E., Ambrosia, V., Toscano, W. M., and Zajkowski, T.: NASA Partners with Forest Service on Fire Mission, Tech. Innovation, 15, 28–30, 2009.
Hintsa, E., Moore, F., Dutton, G., Hall, B., Elkins, J., Gao, R.-S., Watts, L., Thornberry, T., Mclaughlin, R., Ciciora, S., and Fahey, D.: GloPac UCATS and Ozone Dual Beam Spectrophotometer data [data set], available at: https://espoarchive.nasa.gov/archive/browse/glopac (last access: 14 October 2021), 2010.
Hintsa, E., Moore, F., Dutton, G., Hall, B., Nance, D., McClure, A., Elkins, J., Gao, R.-S., Watts, L., Thornberry, T., Rollins, A., Diskin, G. S., Hurst, D., Hall, E., and Jordan, A.: ATTREX UCATS, NOAA O3, Diode Laser Hygrometer, and NOAA ECC Ozonesonde data [data set], available at: https://espoarchive.nasa.gov/archive/browse/attrex (last access: 14 October 2021), 2014.
Hurst, D., Moore, F. Nance, D., Dutton, G. S., Hall, B., and Elkins, J. W.: UCATS 2-Channel Gas Chromatograph (GC) Data, Version 1.0, UCAR/NCAR – Earth Observing Laboratory [data set], https://doi.org/10.26023/HSPN-PGNV-WA0M, 2011.
Jensen, E. J., Jordan, D. E., Fahey, D. W., Newman, P. A., Thornberry, T., Rollins, A., Diskin, G. S., Bui, T. P., McGill, M., Hlavka, D., Lawson, R. P., Gao, R.-S., Pilewskie, P., Elkins, J., Hintsa, E., Moore, F., Mahoney, M. J., Atlas, E., Stutz, J., Pfeilsticker, K., Wofsy, S. C., Evan, S., and Rosenlof, K. H.: The NASA Airborne Tropical TRopopause EXperiment (ATTREX), SPARC Newsletter, 41, 15–24, 2013.
Jensen, E. J., Thornberry, T. D., Rollins, A. W., Ueyama, R., Pfister, L., Bui, T., Diskin, G. S., DiGangi, J. P., Hintsa, E., Gao, R.-S., Woods, S., Lawson, R. P., and Pittman, J.: Physical processes controlling the spatial distributions of relative humidity in the tropical tropopause layer over the Pacific, J. Geophys. Res., 122, 6094–6107, https://doi.org/10.1002/2017JD026632, 2017.
Komhyr, W. D., Barnes, R. A., Brothers, G. B., Lathrop, J. A., and Opperman, D. P.: Electrochemical concentration cell ozonesonde performance evaluation during STOIC 1989, J. Geophys. Res., 100, 9231–9244, https://doi.org/10.1029/94JD02175, 1995.
Kuster, W. C., Goldan, P. D., and Fehsenfeld, F. C.: Controlled environment portable gas-chromatograph for in situ aircraft or balloon-borne applications, J. Chromatography, 205, 271–279, https://doi.org/10.1016/S0021-9673(00)82655-2, 1981.
Moore, F. L., Elkins, J. W., Ray, E. A., Dutton, G. S., Dunn, R. E., Fahey, D. W., McLaughlin, R. J., Thompson, T. L., Romashkin, P. A., Hurst, D. F., and Wamsley, P. R.: Balloonborne in situ gas chromatograph for measurements in the troposphere and stratosphere, J. Geophys. Res., 108, 8330, https://doi.org/10.1029/2001JD000891, 2003.
Navarro, M. A., Saiz-Lopez, A., Cuevas, C. A., Fernandez, R. P., Atlas, E., Rodriguez-Lloveras, X., Kinnison, D., Lamarque, J.-F., Tilmes, S., Thornberry, T., Rollins, A., Elkins, J. W., Hintsa, E. J., and Moore, F. L.: Modeling the inorganic bromine partitioning in the tropical tropopause layer over the eastern and western Pacific Ocean, Atmos. Chem. Phys., 17, 9917–9930, https://doi.org/10.5194/acp-17-9917-2017, 2017.
Pan, L. L., Bowman, K. P., Atlas, E. L., Wofsy, S. C., Zhang, F., Bresch, J. F., Ridley, B. A., Pittman, J. V., Homeyer, C. R., Romashkin, P., and Cooper, W. A.: The Stratosphere-Troposphere Analyses of Regional Transport 2008 (START08) Experiment, B. Am. Meteorol. Soc., 91, 327–342, 2010.
Pan, L. L., Honomichl, S. B., Randel, W., Apel, E. C., Atlas, E. L., Beaton, S., Bresch, J., Hornbrook, R., Kinnison, D., Lamarque, J.-F., Saiz-Lopez, A., Salawitch, R. J., Weinheimer, A. J.: Bimodal distribution of free tropospheric ozone over the tropical western Pacific revealed by airborne observations, Geophys. Res. Lett., 42, 7844–7851, https://doi.org/10.1002/2015GL065562, 2015.
Pan, L. L., Atlas, E. L., Salawitch, R. J., Honomichl, S. B., Bresch, J. F., Randel, W. J., Apel, E. C., Hornbrook, R. S., Weinheimer, A. J., Anderson, D. C., Andrews, S. J., Baidar, S., Beaton, S. P., Campos, T. L., Carpenter, L. J., Chen, D., Dix, B., Donets, V., Hall, S. R., Hanisco, T. F., Homeyer, C. R., Huey, L. G., Jensen, J. B., Kaser, L., Kinnison, D. E., Koenig, T. K., Lamarque, J.-F., Liu, C., Luo, J., Luo, Z. J., Montzka, D. D., Nicely, J. M., Pierce, R. B., Riemer, D. D., Robinson, T., Romashkin, P., Saiz-Lopez, A., Schauffler, S., Shieh, O., Stell, M. H., Ullmann, K., Vaughan, G., Volkamer, R., and Wolfe, G.: The Convective Transport of Active Species in the Tropics (CONTRAST) Experiment, B. Am. Meteorol. Soc., 98, 106–128, https://doi.org/10.1175/BAMS-D-14-00272.1, 2017.
Patra, P. K., Krol, M. C., Montzka, S. A., Arnold, T., Atlas, E. L., Lintner, B. R., Stephens, B. B., Xiang, B., Elkins, J. W., Fraser, P. J., Ghosh, A., Hintsa, E. J., Hurst, D. F., Ishijima, K., Krummel, P. B., Miller, B. R., Miyazaki, K., Moore, F. L., Mühle, J., O’Doherty, S., Prinn, R. G., Steele, L. P., Takigawa, M., Wang, H. J., Weiss, R. F., Wofsy, S. C., and Young, D.: Observational evidence for interhemispheric hydroxyl-radical parity, Nature, 513, 219–223, https://doi.org/10.1038/nature13721, 2014.
Phillips, M. P., Sievers, R. E., Goldan, P. D., Kuster, W. C., and Fehsenfeld, F. C.: Enhancement of electron capture detector sensitivity to non-electron attaching compounds by addition of nitrous oxide to the carrier gas, Anal. Chem., 51, 1819–1825, https://doi.org/10.1021/ac50047a049, 1979.
Plumb, R. A. and Ko, M. K. W.: Interrelationships between mixing ratios of long-lived stratospheric constituents, J. Geophys. Res., 97, 10145–10156, https://doi.org/10.1029/92JD00450, 1992.
Podolske, J. R., Sachse, G. W., and Diskin, G. S.: Calibration and data retrieval algorithms for the NASA Langley/Ames Diode Laser Hygrometer for the NASA Transport and Chemical Evolution Over the Pacific (TRACE-P) mission, J. Geophys. Res., 108, 8792, https://doi.org/10.1029/2002JD003156, 2003.
Proffitt, M. H. and McLaughlin, R. J.: Fast-response dual-beam UV-absorption ozone photometer suitable for use on stratospheric balloons, Rev. Sci. Instrum., 54, 1719–1728, 1983.
Ridley, B. A., Grahek, F. E., and Walega, J. G.: A small high-sensitivity, medium-response ozone detector suitable for measurements from light aircraft, J. Atmos. Ocean. Tech., 9, 142–148, https://doi.org/10.1175/1520-0426(1992)009<0142:ASHSMR>2.0.CO;2, 1992.
Romashkin, P. A., Hurst, D. F., Elkins, J. W., Dutton, G. S., Fahey, D. W., Dunn, R. E., Moore, F. L., Myers, R. C., and Hall, B. D.: In situ measurements of long-lived trace gases in the lower stratosphere by gas chromatography, J. Atmos. Ocean. Tech., 18, 1195–1204, 2001.
Santoni, G. W., Daube, B. C., Kort, E. A., Jiménez, R., Park, S., Pittman, J. V., Gottlieb, E., Xiang, B., Zahniser, M. S., Nelson, D. D., McManus, J. B., Peischl, J., Ryerson, T. B., Holloway, J. S., Andrews, A. E., Sweeney, C., Hall, B., Hintsa, E. J., Moore, F. L., Elkins, J. W., Hurst, D. F., Stephens, B. B., Bent, J., and Wofsy, S. C.: Evaluation of the airborne quantum cascade laser spectrometer (QCLS) measurements of the carbon and greenhouse gas suite – CO2, CH4, N2O, and CO – during the CalNex and HIPPO campaigns, Atmos. Meas. Tech., 7, 1509–1526, https://doi.org/10.5194/amt-7-1509-2014, 2014.
Schauffler, S. M., Atlas, E. L., Blake, D. R., Flocke, F., Lueb, R. A., Lee-Taylor, J. M., Stroud, V., and Travnicek, W.: Distributions of brominated organic compounds in the troposphere and lower stratosphere, J. Geophys. Res., 104, 21513–21535, doi.org/10.1029/1999JD900197, 1999.
Scott, S. G., Bui, T. P., Chan, K. R., and Bowen, S. W.: The Meteorological Measurement System on the NASA ER-2 Aircraft, J. Atmos. Ocean. Tech., 7, 525–540, 1990.
Sweeney, C., Karion, A., Wolter, S., Newberger, T., Guenther, D., Higgs, J. A., Andrews, A. E., Lang, P. M., Neff, D., Dlugokencky, E., Miller, J. B., Montzka, S. A., Miller, B. R., Masarie, K. A., Biraud, S. C., Novelli, P. C., Crotwell, M., Crotwell, A. M., Thoning, K., and Tans, P. P.: Seasonal climatology of CO2 across North America from aircraft measurements in the NOAA/ESRL Global Greenhouse Gas Reference Network, J. Geophys. Res., 120, 5155–5190, doi.org/10.1002/2014JD022591, 2015.
Thames, A. B., Brune, W. H., Miller, D. O., Allen, H. M., Apel, E. C., Blake, D. R., Bui, T. P., Commane, R., Crounse, J. D., Daube, B. C., Diskin, G. S., DiGangi, J. P., Elkins, J. W., Hall, S. R., Hanisco, T. F., Hannun, R. A., Hintsa, E., Hornbrook, R. S., Kim, M. J., McKain, K., Moore, F. L., Nicely, J. M., Peischl, J., Ryerson, T. B., St. Clair, J. M., Sweeney, C., Teng, A., Thompson, C. R., Ullmann, K., Wennberg, P. O., and Wolfe, G. M.: Missing OH reactivity in the global marine boundary layer, Atmos. Chem. Phys., 20, 4013–4029, https://doi.org/10.5194/acp-20-4013-2020, 2020.
Tyson, B. J., Arvesen, J. C., and O'Hara, D.: Interhemispheric gradients of CF2Cl2, CFCl3, CCl4, and N2O, Geophys. Res. Lett., 5, 535–538, https://doi.org/10.1029/GL005i006p00535, 1978.
Vedder, J. F., Inn, E. C. Y., O'Hara, D., Condon, E. P., and Miranda, R. F.: Trace gas measurements during the NASA water-vapor exchange experiment, in: The 1980 Stratospheric-Tropospheric Exchange Experiment, edited by: Margozzi, A. P., NASA Technical Memorandum 84297, 1983.
Waugh, D. W., Crotwell, A. M., Dlugokencky, E. J., Dutton, G. S., Elkins, J. W., Hall, B. D., Hintsa, E. J., Hurst, D. F., Montzka, S. A., Mondeel, D. J., Moore, F. L., Nance, J. D., Ray, E. A., Steenrod, S. D., Strahan, S. E., and Sweeney, C.: Tropospheric SF6: Age of air from the Northern Hemisphere midlatitude surface, J. Geophys. Res., 118, 11429–11441, https://doi.org/10.1002/jgrd.50848, 2013.
Werner, B., Stutz, J., Spolaor, M., Scalone, L., Raecke, R., Festa, J., Colosimo, S. F., Cheung, R., Tsai, C., Hossaini, R., Chipperfield, M. P., Taverna, G. S., Feng, W., Elkins, J. W., Fahey, D. W., Gao, R.-S., Hintsa, E. J., Thornberry, T. D., Moore, F. L., Navarro, M. A., Atlas, E., Daube, B. C., Pittman, J., Wofsy, S., and Pfeilsticker, K.: Probing the subtropical lowermost stratosphere and the tropical upper troposphere and tropopause layer for inorganic bromine, Atmos. Chem. Phys., 17, 1161–1186, https://doi.org/10.5194/acp-17-1161-2017, 2017.
Wilson, K. L. and Birks, J. W.: Mechanism and elimination of a water vapor interference in the measurement of ozone by UV absorbance, Environ. Sci. Technol., 40, 6361–6367, https://doi.org/10.1021/es052590c, 2006.
Wofsy, S., Daube, B., Jimenez-Pizarro, R., Park, S., Kort, E., Gottlieb, E., Pittman, J., and Santoni, G.: QCLS HIPPO data [data set], https://doi.org/10.26023/P1G0-ZSMS-240B, 2011.
Wofsy, S. C.: HIAPER Pole-to-Pole Observations (HIPPO): fine-grained, global-scale measurements of climatically important atmospheric gases and aerosols, Philos. T. R. Soc. A, 369, 2073–2086, https://doi.org/10.1098/rsta.2010.0313, 2011.
Wofsy, S. C., Afshar, S., Allen, H. M., Apel, E., Asher, E. C., Barletta, B., Bent, J., Bian, H., Biggs, B. C., Blake, D. R., Blake, N., Bourgeois, I., Brock, C. A., Brune, W. H., Budney, J. W., Bui, T. P., Butler, A., Campuzano-Jost, P., Chang, C. S., Chin, M., Commane, R., Correa, G., Crounse, J. D., Cullis, P. D., Daube, B. C., Day, D. A., Dean-Day, J. M., Dibb, J. E., DiGangi, J. P., Diskin, G. S., Dollner, M., Elkins, J. W., Erdesz, F., Fiore, A. M., Flynn, C. M., Froyd, K., Gesler, D. W., Hall, S. R., Hanisco, T. F., Hannun, R. A., Hills, A. J., Hintsa, E. J., Hoffman, A., Hornbrook, R. S., Huey, L. G., Hughes, S., Jimenez, J. L., Johnson, B. J., Katich, J. M., Keeling, R. F., Kim, M. J., Kupc, A., Lait, L. R., Lamarque, J.-F., Liu, J., McKain, K., Mclaughlin, R. J., Meinardi, S., Miller, D. O., Montzka, S. A., Moore, F. L., Morgan, E. J., Murphy, D. M., Murray, L. T., Nault, B. A., Neuman, J. A., Newman, P. A., Nicely, J. M., Pan, X., Paplawsky, W., Peischl, J., Prather, M. J., Price, D. J., Ray, E., Reeves, J. M., Richardson, M., Rollins, A. W., Rosenlof, K. H., Ryerson, T. B., Scheuer, E., Schill, G. P., Schroder, J. C., Schwarz, J. P., St. Clair, J. M., Steenrod, S. D., Stephens, B. B., Strode, S. A., Sweeney, C., Tanner, D., Teng, A. P., Thames, A. B., Thompson, C. R., Ullmann, K., Veres, P. R., Vieznor, N., Wagner, N. L., Watt, A., Weber, R., Weinzierl, B., Wennberg, P., Williamson, C. J., Wilson, J. C., Wolfe, G. M., Woods, C. T., and Zeng, L. H.: ATom: Merged Atmospheric Chemistry, Trace Gases, and Aerosols, ORNL DAAC, Oak Ridge, Tennessee, USA, https://doi.org/10.3334/ORNLDAAC/1581, 2018.