Editorial Type:
Article
Article Type:
Research Article

A Case Study of Stratospheric Ozone Transport to the Northern San Francisco Bay Area and Sacramento Valley during CABOTS 2016

Jodie Clark Center for Applied Atmospheric Research and Education, San Jose State University, San Jose, California

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Sen Chiao Center for Applied Atmospheric Research and Education, San Jose State University, San Jose, California

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https://orcid.org/0000-0001-7117-1577
Print Publication:
01 Dec 2019
DOI:
https://doi.org/10.1175/JAMC-D-18-0322.1
Page(s):
2675–2697
Free access

Abstract

The California Baseline Ozone Transport Study (CABOTS) was a major air quality study that collected ozone measurements aloft between mid-May and mid-August of 2016. Aircraft measurements, ground-based lidar measurements, and balloon-borne ozonesondes collected precise upper-air ozone measurements across the central and Southern California valley. Utilizing daily ozonesonde data from Bodega Bay, California, and Modern-Era Retrospective Analysis for Research and Applications, version 2 (MERRA-2), reanalysis data for 25 July to 14 August 2016, three stratospheric intrusion events are identified over Northern California influencing air masses above Bodega Bay and Sacramento simultaneously. Calculated percent daily changes in afternoon ozonesonde observations indicate increasing ozone concentrations from the point of likely stratospheric air injection with the arrival of higher potential vorticity, confirmed by ensemble back trajectories. An analysis of the onsite surface monitoring ozone data indicates ozone increases in the observations for dates of plausible low-level stratospheric air influence. Further, a comparison of Bodega Bay surface ozone observations and 14 Sacramento Valley nonattainment zone surface sites show that the surface ozone observed at the higher-elevation surface sites in the lower Sierra Nevada foothills were positively correlated with elevated ozone captured by the ozonesondes within the lowest 0.5–1 km. The strongest correlations observed (~0.61) were between elevated Bodega Bay ozonesonde data and the Placerville (~612 m) afternoon surface ozone data, an indication that these regions separated by 200 km would be influence by the same ozone source. A comparison of daily changes in afternoon ozone show that the two locales often experience similar daily ozone increases or decreases. While this study leads to a basic quantification of stratospheric influence on surface ozone in the Sacramento nonattainment zone, a future campaign that examines ozone and winds aloft at both locales is suggested to improve the quantification of stratospheric ozone.

© 2019 American Meteorological Society. For information regarding reuse of this content and general copyright information, consult the AMS Copyright Policy (www.ametsoc.org/PUBSReuseLicenses).

Corresponding author: Sen Chiao, sen.chiao@sjsu.edu

Abstract

The California Baseline Ozone Transport Study (CABOTS) was a major air quality study that collected ozone measurements aloft between mid-May and mid-August of 2016. Aircraft measurements, ground-based lidar measurements, and balloon-borne ozonesondes collected precise upper-air ozone measurements across the central and Southern California valley. Utilizing daily ozonesonde data from Bodega Bay, California, and Modern-Era Retrospective Analysis for Research and Applications, version 2 (MERRA-2), reanalysis data for 25 July to 14 August 2016, three stratospheric intrusion events are identified over Northern California influencing air masses above Bodega Bay and Sacramento simultaneously. Calculated percent daily changes in afternoon ozonesonde observations indicate increasing ozone concentrations from the point of likely stratospheric air injection with the arrival of higher potential vorticity, confirmed by ensemble back trajectories. An analysis of the onsite surface monitoring ozone data indicates ozone increases in the observations for dates of plausible low-level stratospheric air influence. Further, a comparison of Bodega Bay surface ozone observations and 14 Sacramento Valley nonattainment zone surface sites show that the surface ozone observed at the higher-elevation surface sites in the lower Sierra Nevada foothills were positively correlated with elevated ozone captured by the ozonesondes within the lowest 0.5–1 km. The strongest correlations observed (~0.61) were between elevated Bodega Bay ozonesonde data and the Placerville (~612 m) afternoon surface ozone data, an indication that these regions separated by 200 km would be influence by the same ozone source. A comparison of daily changes in afternoon ozone show that the two locales often experience similar daily ozone increases or decreases. While this study leads to a basic quantification of stratospheric influence on surface ozone in the Sacramento nonattainment zone, a future campaign that examines ozone and winds aloft at both locales is suggested to improve the quantification of stratospheric ozone.

© 2019 American Meteorological Society. For information regarding reuse of this content and general copyright information, consult the AMS Copyright Policy (www.ametsoc.org/PUBSReuseLicenses).

Corresponding author: Sen Chiao, sen.chiao@sjsu.edu
Keywords: Air quality

1. Introduction

Stratospheric intrusions (SI) transport ozone-rich stratospheric air to the lower troposphere, intermittently enhancing ozone (O3) concentrations in the lower troposphere (e.g., Cooper et al. 2001; Stohl et al. 2003; Lin et al. 2012, 2015; Tarasick et al. 2019). The deep descent of stratospheric air has been defined as that which crosses the dynamical tropopause and travels to 700 hPa pressure level within 5 days (Bourqui and Trépanier 2010). The photochemical lifetime of O3 in the free troposphere is about 22 days (Stevenson et al. 2006). Since the nonconservative processes known to transport stratospheric air to the troposphere are on the order of a few days, such as the turbulence caused by strong wind shear typically found in tropopause folds, stratospheric O3 (stratO3) can significantly influence the background O3 (bgO3) in the free troposphere uninfluenced by anthropogenic emissions and the surface O3 (sfcO3) concentration (Bourqui and Trépanier 2010). Nevertheless, the challenge is to identify and quantify the influence of stratO3 and to what extent stratO3 intrudes into the troposphere to influence the sfcO3 pollution above the health-based limit (e.g., Ding and Wang 2006; Hsu and Prather 2009; Langford et al. 2009).

For decades potential vorticity (PV) and layered structures in O3 profiles have been used to identify stratospheric air masses (e.g., Danielsen et al. 1987; Oltmans et al. 1996; Roelofs et al. 2003; Škerlak et al. 2014). When defining the height of the tropopause, it is well established that the sharp rise in O3 corresponds well with the strong rise in PV (Trickl et al. 2014). One cause of variability to the tropopause height is Rossby wave propagation and breaking, which can lead to a SI of air with high PV into the subtropical and midlatitude upper troposphere (e.g., Waugh 2005; Ryoo et al. 2008; Bourqui and Trépanier 2010). Bourqui and Trépanier (2010) further categorized three distinct phases of an SI as the transport of stratospheric air across the tropopause; the free descent with minimal tropospheric mixing; and the quasi-horizontal dispersion into the lower troposphere.

Prior studies have suggested that the west coast of North America is a hot spot not only for SI, but deep SI, allowing for mixing into the boundary layer (BL) (e.g., Wernli and Bourqui 2002; Lefohn et al. 2012; Lin et al. 2012; Škerlak et al. 2014; Ryoo et al. 2017). Of the mass fluxes that cross the tropopause above California, 10% continue to cross the 700 hPa level and 5% cross the 800 hPa level (Škerlak et al. 2014). Although it has been known that SI occur more frequently in the Northern Hemisphere (NH) winter and early spring due to the position of the jet streams, the stratO3 intrusion through deep SI instances occur above California in each season, and have been noted to reach the planetary BL similarly (Škerlak et al. 2014). Lin et al. (2012) found suggestions of strong stratO3 in the Sierra Nevada range. They suggest more measurements be recorded at these rural sites to gain insight into the influence of stratO3 on sfcO3 in the local urban area through a greater understanding of stratO3 influence on the bgO3 concentrations within the region.

From the air quality standards perspective, it is essential to investigate the quantitative relationship between deep SI and sfcO3 concentrations. Without convective processes or strong wind shear, the mixing of the intruded stratospheric air into tropospheric air would be a very slow process, possibly remaining stratospheric in nature for 1–2 weeks (Trickl et al. 2014). The downward transport of injected stratO3 from the lower troposphere to the surface could be further aided by wave activity, turbulence, or shear created by downslope winds. For instance, Langford et al. (2009) found that during the springtime in the metropolitan area of Denver, Colorado, SI brought extremely dry, O3-rich air to the surface sites that well exceeds the National Ambient Air Quality Standard (NAAQS). Yet evidence of the SI passed after just a few hours, demonstrating that the commonly performed weekly sampling of tropospheric O3 does not provide adequate data (Langford et al. 2009).

Quantifying the actual amount of stratO3 that contributes to tropospheric O3 remains a topic of interest. The layered structures found in vertical O3 profiles measured by ozonesondes is not reproduced well in many global and regional tropospheric chemical transport models (Roelofs et al. 2003; Lin et al. 2012). The models struggle further with deciphering the impacts of stratO3 influence on the sfcO3 observations (Lin et al. 2012). To capture the full impact of SI on bgO3 and sfcO3 conditions, daily measurements would be beneficial to the atmospheric chemistry and air quality communities and would contribute to strengthening model accuracy of forecasted O3 predictions.

Using the daily upper-air O3 measurements collected during the California Baseline Ozone Transport Study (CABOTS) 2016, this research aims to investigate SI that occurred over Northern California in relation to sfcO3 over the Sacramento area. Liu et al. (2009) found that the correlation strength between ozonesonde measurements decreased by a factor of e in the stratosphere over distances of 1000–2000 km and in the troposphere over distances of 500–1000 km. Oltmans et al. (2008) found the observed air entering from the Pacific in the lower troposphere (1–5 km) above the marine BL provides a good picture of the bgO3 content. Therefore, coastal ozonesonde measurements would give a good indication of elevated O3 values 100–200 km eastward elevated above the Sacramento nonattainment zone.

Using high temporal density upper-air O3 measurements, the spatial and temporal characteristics of SI induced sfcO3 variability will be revealed. The primary objective of this study is to advance our understanding of stratO3 influence during the passage of a SI over Northern California and aims to show the vertical descent of stratO3 to the surface is plausible following the passage of an SI into the middle troposphere. This study is unique to tell the tale of the vertical daily variability in O3 concentrations entering the central California coast by calculating the daily percent changes in O3 for a continuous 21 days of ozonesonde measurements, recognizing trends with time of increasing O3 concentrations following from the region of stratospheric air intrusion toward the surface. A secondary objective of this study is to discover a correlation between the stratO3 influencing BL O3 at the North Bay area coastal region with the sfcO3 pollution observed in the Sacramento nonattainment zone and the lower Sierra Nevada foothills to quantify stratO3 contributing to nonattainment.

Section 2 depicts the datasets utilized. In section 3, the SI events for analysis are defined. Section 4a confirms the SI events with HYSPLIT back trajectories and ozonesonde analysis. The trekking of stratO3 with time and surface ozone correlation results and discussion wrap up section 4. Section 5 states the conclusions of the study and the ideas for further improvement. This study is largely based on the thesis research of Clark (2018), which is repeated in this paper with permission.

2. Data collection

a. Ozonesonde measurements

It is suggested by Lin et al. (2015) that weekly ozonesonde measurements at Trinidad Head, California, and Boulder, Colorado, are inadequate to capture the actual temporal variability of mean midtropospheric O3 in spring. The near-daily ozonesondes launched from Bodega Bay, California, contribute to the CABOTS campaign objective of bringing insight to the vertical daily variability of bgO3 as it enters the West Coast, which would include those variations of bgO3 due to SI contributing to this study’s primary objective. As the shallow nocturnal BL heights grow to daytime heights, the higher O3 concentrations aloft begin to mix down in the elevated daytime BL. This, along with the daytime photochemical production of O3, leads to maximum sfcO3 concentrations in the afternoon (Parrish et al. 2010). Therefore, the Bodega Bay ozonesondes were released at 2100 UTC (1400 local time) from 38.31869°N, 123.07197°W at an elevation of 12 m above sea level, and 200 m directly east from the coastline. Prior to this study, vertical O3 data had not been collected along the central coast of California making the CABOTS data a valuable new dataset.

A total of 86 near-daily ozonesondes were launched by the SJSU launch team at Bodega Bay, collecting finescale vertical O3 data throughout the troposphere and into the lower stratosphere. The ozonesonde launch site is shown in Fig. 1a. A time–height cross section plot, as shown in Fig. 2a, depicts the 100-m vertically averaged O3 concentrations measured during the entire field study, late May to early August 2016. The frequent occurrence of high O3 concentrations in the upper troposphere was clearly recognizable within the data. On occasion, relatively high O3 concentrations extend down from the tropopause toward the lower troposphere, impacting below 4 km (Fig. 2a).

Fig. 1.
Fig. 1.

(a) Location of the 15 surface ozone monitoring stations across Northern California and the Bodega Bay ozonesonde launch site. (b) 3D layout of the Sacramento surface stations with location names.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Fig. 2.
Fig. 2.

Bodega Bay near-daily ozonesonde observations. Color scale concentrations from 0 to 160 ppb. (a) all CABOTS data, 2016. (b) 25 Jul–16 Aug 2016.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

In the lower levels, the observed O3 values would include O3 mixing upward from the surface, long-range transport, and mixing from upper-level layers due to SI. In the lower 2 km, multiple occurrences of O3 concentrations greater than 70 ppb were observed (Fig. 2a). Figure 2b displays the O3 measurements collected during the period of 25 July through 16 August 2016. During this defined case study period, the air quality index for sfcO3 pollution in the Sacramento nonattainment zone was classified as moderate to unhealthy. Successive accurate ozonesonde launches were performed collecting quality daily observations of coastal O3 aloft throughout a 15 km vertical column, except for 16 August where complications allowed for data up to 5 km.

b. MERRA-2 reanalysis

MERRA-2 reanalysis data have been recognized as a valuable dataset and tool in the use of identifying SIs (Knowland et al. 2017). Therefore, this study utilizes this global dataset for analysis of 250 hPa geopotential height and wind speed over a domain that covers the eastern North Pacific Ocean and most of North America, and for a vertical cross-section analysis of PV and wind speed to show the occurrence of the SI events over Northern California during a period of 25 July–13 August 2016. The MERRA-2 model dataset is composed of 72 hybrid sigma–pressure levels with a resolution of 0.5° latitude × 0.625° longitude, and a 3-hourly time stamp.

c. Surface monitoring stations

Data from 15 sfcO3 monitoring stations were used for analysis of the unhealthy air conditions in the Sacramento nonattainment zone (Table 1). SfcO3 data were provided by the California Air Resources Board (CARB) and included the hourly average sfcO3 values observed during the period of the CABOTS project. Observations from 14 surface sites were used within this case study (Fig. 1b). The sfcO3 data for Bodega Bay were provided by the Bay Area Air Quality Management District (BAAQMD). This dataset included sfcO3 values observed for every minute, which were averaged to hourly O3 data for 25 July–17 August 2016.

Table 1.

Surface ozone monitoring sites locations.

Table 1.

3. Defining three SI cases

In general, the dynamic tropopause is defined when PV is equal to 2 PVU (1 PVU = 10−6 m2 s−1 K kg−1), but accepted values range from 1 to 5 PVU with the lowest values indicative of a deep SI that captures the streamers associated with the fold (Cox et al. 1997). Large PV values in the troposphere are regarded to be linked to the stratosphere, and a value of 5.0 PVU would mark a definite boundary between stratospheric and tropospheric air. In this study, a value of 1.5 PVU was used to indicate the height of the tropopause near folds, and a value of 1.0 PVU indicates the deeper intrusion of stratospheric air below the tropopause into the troposphere.

Vertical cross sections were performed to analyze the placement of the upper-level jet stream and the arrival of the high PV values to the Bodega Bay (BBY) vertical column of air. Figures 3–5 show the PV and wind speed values along three different cross sections: 1) a vertical cross section along the U.S. West Coast from a point in the Gulf of Alaska (50.0°N, 132.0°W) crossing through Bodega Bay and to a point off the southern west coast of Baja California (25.0°N, 116.0°W); 2) a vertical cross section from southern British Colombia (50.0°N, 118.0°W) to the southeast along the Cascade Mountain Range, crossing through BBY and into the Pacific Ocean (25.0°N, 127.0°W); and 3) a longitudinal vertical cross section starting in the Pacific Ocean off the California west coast (35.9°N, 134.0°W) to a point almost directly westward in the Pinyon Creek Canyon of Utah (40.0°N, 112.0°W) allowing the data to pass through BBY and Placerville, California. In the upper-left-hand corner, the figures include the 250 hPa geopotential height and wind speed to link the regions of higher PV with the known signatures of tropopause folding, the upper-level jet stream and jet streaks, the synoptic scale features of upper-level fronts, and the low pressure systems across the domain (Lin et al. 2012; Škerlak et al. 2014). Since ozonesonde data were only collected for 2100 UTC, the MERRA-2 data shown are for the day of the SI event into the BBY region, and the proceeding and following days at this time stamp.

Fig. 3.
Fig. 3.

MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections for (left) 26 Jul, (middle) 27 Jul, and (right) 28 Jul 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Fig. 4.
Fig. 4.

MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections on (left 4 Aug, (middle) 5 Aug, and (right) 6 Aug 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Fig. 5.
Fig. 5.

MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections on (left) 9 Aug, (middle) 10 Aug, and (right) 11 Aug 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

As of 25 July 2016, the 250 hPa geopotential heights show the presence of a developed upper-level closed low over southern Alaska with a broad trough across the Gulf of Alaska. To the south was an upper-level cutoff low that elongated and separated toward the east of Hawaii, while a small upper-level closed low perturbance lifts into the jet stream. A broad upper-level ridge of high pressure extended from the Pacific Ocean, across the lower United States and Mexico; engulfed was an upper-level cutoff low centered between the southern tip of Baja California and the Hawaiian Islands on a westward track. The jet stream propagated across the Pacific entering the Pacific Northwest and Northern California, zonally across the upper-level high pressure ridge.

By 26 July 2016 at 2100 UTC, the upper-level closed low over Alaska has deepened. Only a small trace of the upper-level cutoff low remained to the north of Hawaii (Fig. 3). The broad upper-level ridge of high pressure that extended from the desert southwest builds slightly at the U.S. West Coast and remained over the eastern Pacific and southern United States. The jet stream remained in a similar location with a zonal entrance across the Pacific Northwest. Some embedded shortwave troughs from the once-strong embedded upper-level cutoff low to the north of Hawaii progressed upstream, one remained just offshore of Northern California (Fig. 3). The jet-stream pushes farther northward as the high pressure ridge builds over the coast; the southern cutoff low continued the westward track toward Hawaii.

The first SI (SI 1) of interest into the elevated air above Northern California, recognized in the ozonesonde data, began on the afternoon of 27 July 2016 and remained present into 28 July 2016. Figure 3b indicates that an intrusion of stratospheric air occurred with the southern westward-tracked upper-level cutoff low, and a streamer from the low progressed to the northeast and influenced the air mass elevated above BBY as the upper-level ridge built over the four corners (Center for Atmospheric Research and Education 2016). The high PV air mass progressed westerly across the state of California and through, influencing the air mass elevated above BBY and the Sacramento nonattainment zone represented by Placerville into the hours of 28 July 2016 as high PV separates from the tropopause and an enclosed region of high PV remained at about 8 km (Fig. 3c). The intrusion of stratospheric air into the 7–14 km vertical column elevated above BBY and Placerville passed through by 29 July 2016.

Over the course of the next week, the upper-level ridge of high pressure to the south weakened, multiple regions of high and low pressure circulated around the open Pacific, and the jet stream diverged into two weaker jets: one across the Pacific Ocean and one to the north. The southern upper-level cutoff low began a northwestward trek to the north of Hawaii and toward the southern westerly jet stream across the open Pacific. Along the jet stream to the north, three upper-level closed lows dropped into Alaska and progressed westward across the Gulf and into southern Canada.

By 2100 UTC 4 August 2016, as the upper-level high pressure ridge at the West Coast weakened. The southern jet stream crossing into the United States, which extended from the upper-level cutoff low across the Pacific, had broadened from Southern California to northern Oregon from the southwest (Fig. 4). The upper-level cutoff low to the north of Hawaii now exhibited a positive tilt as a powerful shortwave trough elongated the trough axis to the west. As higher pressure built in the Gulf of Alaska, the third upper-level closed low had progressed along the coast of British Columbia and approached northern Washington, also influenced with a shortwave trough. Figure 4 indicates the height of the 1.5 PVU tropopause over California had lowered to near 9 km while the 2.0 PVU remained elevated as high as 14 km above BBY and Placerville.

As shown in Fig. 4, multiple regions of 1.0–2.0 PVU extended into the midtroposphere at 8–4 km and trekked into the region from the west with short-wave troughs along the jet stream. The second SI (SI 2) of interest recognized in the ozonesonde data occurred with the lowering of the 2.0 and 5.0 PVU line elevated above the BBY region early on 5 August 2016. The closed upper-level low to the north digs slightly deeper along the coast of British Columbia and the circulation separated from the flow of the upper-level cutoff low to the north of Hawaii. The embedded short-wave trough began to swing through the upper-level closed low, and the trough deepened. The jet stream strengthens and traverses across the middle of California in a northeasterly direction, crossing above the North Bay area, Sacramento, and Tahoe. By 2100 UTC 6 August 2016 the center of the closed low pressure was above northern Washington and trekking southward, the embedded short-wave trough swung into the center of the trough axis just off the West Coast (Fig. 4c), with an extension of the 1.0 PV line to as low as 700 hPa. The upper-level cutoff low remained circulating over the open Pacific Ocean to the north of Hawaii, with a strong jet forming to its north along the Aleutian Islands as a center of low pressure was forming and a small high pressure ridge was present in the Gulf of Alaska.

As the jet progressed over the upper-level ridge of high pressure in the Gulf of Alaska, the flow of the upper-level cutoff low and closed low was in unison once more. Over the next 24 h another short-wave trough progressed through, once again strengthening and separating the flow of the upper-level lows. By 2100 UTC 8 August 2016, the center of the upper-level closed low has moved southward above western Washington and Oregon, with an embedded short-wave trough forming a strong upper-level frontal boundary perfect for tropopause folding. The jet core was elevated at 10–12 km above the region of interest. Offshore to the northwest of the jet core, the 5.0 PVU line extended down to 10 km in a southeasterly direction, and the 1.0 PVU extended toward 5 km in a narrow strip (Fig. 5a). To the northeast the 5.0 PVU line extended down to 8 km though the center of closed low, with 1.0 PVU extended toward 2.0 km through the center and across the frontal boundary (Fig. 5b).

By 9 August 2016, the upper-level ridge of high pressure remained in the Gulf of Alaska and the strong upper-level jet stream traversed along hugging the Gulf of Alaska. Figure 5 shows the center of the upper-level closed low progressed to the east above Washington and Oregon and exhibited an elongated positive tilted trough, or upper-level front, extended off the west of Southern California. The large upper-level front passed through BBY in the late morning hours of 9 August 2016; the third SI (SI 3) of interest recognized in the ozonesonde data. While the strong upper-level front passed though quickly, the closed low moves slowly to the east, squeezed as an upper-level high pressure ridge was present above the desert southwest and the southeast states. Figure 5 indicates that behind the front to the northwest, west, and even to the northeast of the upper-level closed low, many 1.0 PVU and some 1.5 PVU air masses were present elevated between 8 and 2 km. The front swings though, deepening the base of the trough to pass over Southern California. The higher values of PV stream in from the northwest around the jet core, and the 1.0–2.0 PVU lines extended into the midtroposphere. By 2100 UTC 9 August 2016 the 5.0 PVU line drops to near 10 km elevated above the width of California within the region of interest, and the 1.0 PVU line drops to near 7 km (Fig. 5).

By 2100 UTC 10 August 2016, the upper-level trough broadened over the western United States. The streamer of SI 3 extended from the tropopause above Nevada and Utah, across the region of interest, and out into the lower air mass elevated above the coastal ocean (Fig. 5c). The streamer remained present into the morning hours of 11 August 2016. The trough lifted by 2100 UTC 11 August 2016 and the ridge of high pressure progressed onshore over the western United States. The tail end of the streamer cut off from the tropopause and remained elevated 2–4 km above BBY, extended to the west-southwest over the coastal waters (Figs. 5b,c). The stratospheric air mass descended toward the surface over the next hours as the area was influenced by higher pressure (Center for Atmospheric Research and Education 2016).

During the defined time periods, the three SIs cross over and influence both the North Bay area and the Sacramento nonattainment zone (SAC). From the comparison of MERRA-2 PV longitudinal cross sections in Figs. 3c, 4c, and 5c, the same SI of interest were noted above BBY and SAC. These similarities to the elevated air masses define the regions as comparable, especially above 2 km. Therefore, BBY ozonesonde measurements would give an indication of vertical O3 structure above SAC. It is important to note that the PV values in the lower 3 km are prominent offshore during all hours analyzed. While the diabatic heating effect can be a dominant factor to produce high PV if air is moist in the low levels of the troposphere (< 3 km), this has shown to not be the case if a region also exhibits low specific humidity (Hoskins et al. 1985). From the Center for Atmospheric Research and Education (2016) the air of this region was quite dry during the period, especially above the marine layer. Inland, the high PV values appear at the surface generally between 0600 and 1500 UTC in occurrence with the land–sea breeze circulation and other mesoscale complexes.

4. Method and analysis

a. Confirming SIs with HYSPLIT and CABOTs data

The NOAA HYSPLIT archive back-trajectory model was run to confirm the directionality of the air as it approached BBY followed along the path of the high PV air masses. The model simulations used the 0.5° resolution GFS global model dataset with an isentropic vertical velocity calculation ensemble method to evaluate the air entering the elevated region above the BBY launch site located at 38.318°N, 123.071°W. Produced from the HYSPLIT model (Stein et al. 2015), Figs. 6–8 confirm the air that entered the vertical column above BBY at 2100 UTC on the dates of 27 July, 5 August, and 9 August 2016 followed a similar 4-day path as the proposed high PV SI events defined in section 3: from the south and from the west; from the west, southwest, and northwest; from the strong low pressure system to the north.

Fig. 6.
Fig. 6.

NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 27 Jul 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Fig. 7.
Fig. 7.

NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 5 Aug 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Fig. 8.
Fig. 8.

NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 9 Aug 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

The multiple elevations analyzed during the back-trajectory analysis (Figs. 6–8) link the arrival of high PV (Figs. 3–5) with the afternoon O3 increases calculated for the corresponding dates (Fig. 9). The daily variation of O3 by height was evaluated to visualize the influence and progression of the dry, O3-rich stratospheric air masses with time. Utilizing BBY ozonesonde observations, the daily percent changes in O3 were calculated for the 15 km vertical air column from one afternoon to the next for 25 July–14 August. Equation (1) shows the simple calculation for the daily O3 percent changes for each 100-m average O3 value:
ΔO3%=[⁡(O3ppbf−O3ppbi)|O3ppbi|]⁡(100).
Fig. 9.
Fig. 9.

(a) Calculated percent change in O3 from the BBY afternoon ozonesonde 100-m average values from day to day, increases in O3 for SI 1 and plausible low-level intrusions (P) are marked where a, b, and c specify which cross sections indicate high PV to the region, 26 Jul–4 Aug. (b) Calculated percent change in O3 from the BBY afternoon ozonesonde 100-m average values from day to day, increases in O3 for SI 2 and SI 3 with plausible low-level intrusion (P3) are marked where a, b, and c specify which cross sections indicate high PV to the region, 4–14 Aug.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Figure 9 shows the daily percent changes in measured BBY O3 for the period. Within the region of the tropopause (10–12 km) some of the largest daily percent changes in O3 occurred. The elevations are marked in Fig. 9 by a number and a letter indicating an intrusion of stratO3 into the region. The number indicates the SI case and the letter corresponds to the cross section that exhibited the high PV air masses (Figs. 3–5). The greatest change in O3 observed from SI 1 was an increase of 258% to 86 ppb at 10.9 km on 27 July 2016 (Fig. 9a). At this elevation, the top-left image of Fig. 6 shows the back trajectories come from two distinct regions at very different paces. It is estimated about half the trajectories approach from the west near Hawaii along the jet stream, while the other half progresses slowing up from the south near northern Mexico with the building of high pressure. At 11 km on 5 August 2016, the observed O3 value was 198 ppb, a 236% increase from the afternoon prior (Fig. 9b). The top-left image of Fig. 7 indicates that the air entering this region converges early above the open pacific then treks westward along the jet stream. The greatest of all the daily O3 percent changes for this study was observed at 11.1 km on 9 August, an increase of O3 by 415% from the afternoon prior to 169 ppb (Fig. 9b). The back trajectories of the top-left image in Fig. 8 indicate the air entering BBY at this elevation strongly follow the circulation of the low pressure system to the north.

Significant O3 increases were observed in the midtroposphere as well. At the height of 6–8 km, the MERRA-2 PV cross section showed a cutoff of high PV beginning on 27 July 2016 (Fig. 3). The BBY ozonesonde captured daily O3 increases that ranged from 90% to 110%, a near-40-ppb increase (Fig. 9a). Afternoon O3% increases of near 100% were observed near 7 km on 5 August 2016 (Fig. 9b) and an indication on 1.0 PVU was present (Fig. 4b). The 5 km ensemble back trajectories in the lower left of Fig. 7 indicate air reaching this elevation is approaching from many directions. Some of the air came from the north elevated above British Columbia on 2 August 2016 at the same time as an upper-level low progressed through the region described briefly in section 3. This indicates the arrival of sratO3 into the region of interest. On 9 August increases in O3 occurred throughout most of the vertical column, the 1–7 km of up to 155% (Fig. 9b). A region of 1.0 PVU was present in the 4–5 km vertical column of Fig. 5.

b. CABOTs data: Tracking SI influence with time

As previously noted, SI 1 occurred with a relatively high tropopause height of 14 km (Fig. 3). The ozonesonde data captured the beginning of this event as an increase of observed O3 through a long vertical column between 6 and 14 km on 26–27 July 2016 (Fig. 9a). Smaller O3 increases were observed at the same altitudes on 28 July as the intrusion remained (Fig. 9a). While SI 1 was not likely the cause of any lower-level increases in O3, the progression of increasing O3 with time from SI 1 is examined in Fig. 9a. Three other possible low-level intrusion cases (P) are marked in Fig. 9a. While it is likely that these low-level increases of O3 that appear to descend to the surface with time are linked with low pressure systems to the north, uncertainty remains, and the cases should be closer examined.

Figure 9b follows the progression of the increasing O3 with time associated with SI 2 and SI 3. As each SI is associated with a lowering of the tropopause and an intrusion of stratospheric air into the midtroposphere, the progression of increasing O3 is tracked from multiple altitudes. BBY ozonesonde percent change data captured increases in O3 from 4 to 5 August observed through the 7–14 km vertical column with the arrival of SI 2 (Fig. 9b). SI 3 is discussed in greater detail as stratO3 likely influence the overnight sfcO3 concentrations.

On 9 August 2016, with the arrival of the strong upper-level front, increases in observed O3 occurred throughout most of the vertical column, excluding the upper and the lower one kilometer. Figure 8 shows that the air between 2 and 6 km follows the same path as the upper-level intrusion, but the increases in O3 observed in Fig. 9b are not represented by high PV in the vertical cross sections of Fig. 5. The 4–5 km ensemble back trajectories for 9 August in Fig. 8 indicate that some of the air entering BBY had previously passed through BBY on 6 August at a higher elevation between 4 and 8 km. Therefore, Fig. 9 indicates the decent of stratO3 with time from the ozonesonde observations of high PV on 6 August into 6 km as the embedded short-wave trough passed through the base of the trough of the enclosed upper-level low (Fig. 4). By 10 August 2016 the low-level tail of SI 3 influenced the region (Fig. 5) and low-level O3 increases were observed. By 11 August, the tail of SI 3 lifted and cut off from the upper SI 3 event and remains elevated above BBY. With the presence of higher pressure to the region, the high PV air mass began to descend toward the surface, reaching near 500 m the afternoon of 12 August and influencing the sfcO3 by 13 August (Fig. 9b). The arrival of the strong frontal passage allowed for the deep descent of stratospheric air into lowest levels of the vertical column elevated above BBY.

c. BBY and SAC maximum daily 8-h average SfcO3 analysis

The BBY sfcO3 monitoring data provided by BAAQMD reflects similar increases with time as those inferred from the probable near-surface influence perceived in the SI 3 event at the end of the period (Fig. 9b). Also, while not fully discussed, a downward trend of increasing O3 can be inferred in the BBY sfcO3 from the proposed lower-level stratospheric influence from upper-level closed lows pointed out in Fig. 9a. Figure 10a shows the calculated BBY surface maximum daily 8-h average (MDA8) O3 values for 25 July–17 August 2016. Along with being a value of interest to the EPA, these averages are evaluated to reduce the effects of local pollution on the observed sfcO3 values (Parrish et al. 2010). The observed MDA8 O3 concentrations at BBY illustrate a small daily range of 2–10 ppb and the mean MDA8 O3 value observed at BBY during the case study was near 20 ± 5 ppb (Fig. 10a).

Fig. 10.
Fig. 10.

(a) Classic boxplot for the calculated maximum daily 8-h average ozone at BBY for 25 Jul–17 Aug 2016, local hour 0 through 23, orange bar = daily mean, black bar = daily median. (b) Onsite min-by-min BBY sfcO3 observations 30 Jul–4 Aug. (c) Onsite min-by-min BBY sfcO3 observations 10–15 Aug. Green boxes indicate dates and times that the stratO3 is suggested to have influenced the sfcO3 concentrations based on the ozonesonde analysis.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

The green boxes in Fig. 10a indicate dates that the stratO3 from 2 proposed SI events and the defined SI 3 event influenced the sfcO3 concentrations according to the daily percent change in O3 analysis of BBY ozonesondes (Fig. 9). Figures 10b and 10c show a 5-day period of minute-by-minute sfcO3 data collected on site. These images were created during the field study and included the time of the proposed influence of stratO3, also enclosed in green boxes. As the stratO3 from SI 3 reached the lowest 1 km (Figs. 9a,b), the onsite surface observations lack the presence of the typically expected overnight/early morning minimum sfcO3 observation. StratO3 from SI 3 contributed to the 12 August late night and 13 August early morning O3 observations as a maximum in sfcO3 was reached for the 2-day period (Fig. 10c), with possible influence into the afternoon hours as ozonesonde data did indicate an increase in its lowest levels (Fig. 9b). SfcO3 influence from a proposed SI into the lower levels occurred early morning of 2 August from the initial influence of the upper-level closed low to the northwest (Fig. 10b). The final passing of the upper-level closed low to the northeast likely influenced sfcO3 concentrations on the night of 3 August, and the early morning of 4 August. Again, the time period exhibited little daily variation in the sfcO3 values (Fig. 10b).

Within SAC, the surface MDA8 O3 were calculated for 14 surface monitoring stations located across the southern Sacramento Valley and the local lower Sierra Nevada foothills. The monitoring sites were subcategorized into three groups based on elevation; high, middle, and low. These were defined by the elevation of the chosen sites accordingly: surface stations located (i) above 108 m, (ii) between 108 and 47 m, and (iii) below 47 m. This conveniently groups the sfcO3 monitoring sites similarly by longitude. The high-elevation sites are located farthest east while the low-elevation sites are located farthest west (Fig. 1). Figure 10 shows the calculated MDA8 O3 values for each SAC surface monitoring site along with the BBY values for an easy comparison.

The mean MDA8 O3 observations were compared among all the surface monitoring sites. O3 observations at the inland SAC surface sites generally were greater than that observed at BBY and were representative of a larger daily range in MDA8 O3. In general, the mean MDA8 O3 concentrations were greatest at the highest elevation site and decrease with a corresponding decrease in height (Fig. 11). A mean MDA8 O3 of near 70 ppb was observed during the case study period at Grass Valley, typical of a site driven by local photochemical O3 production rather than long-range transport of O3. Similarly, mean O3 concentrations observed at the Colfax and Placerville sites were around 70 ppb (Fig. 11a). This observation alone creates a clear picture of the unhealthy surface air conditions and nonattainment of the region. The high-elevation monitoring sites observed mean MDA8 O3 values ranging between 50 and 80 ppb for the study period (Fig. 11a). The mean MDA8 O3 observations at the mid- and low-elevation sites remained below the NAAQS. The midelevation monitoring sites observed concentrations for the period ranging from 30 to 60 ppb and the low-elevation monitoring sites ranging from 20 to 50 ppb (Figs. 11b,c). Dissimilar from the observations at BBY, the mean MDA8 O3 values at the SAC surface sites were typically greater than or equal to the median (Fig. 11). The greatest exceptions occurred at the high-elevation sites of Grass Valley and Placerville (Fig. 11a).

Fig. 11.
Fig. 11.

Calculated surface MDA8 O3 concentration boxplots for 25 Jul–17 Aug 2016 for the SAC and BBY: (a) high-, (b) mid-, (c) low-elevation surface sites; colored bar = daily mean, black bar = daily median.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

The daily range of MDA8 O3 observed among the SAC surface monitoring sites during the case study period were analyzed and compared with BBY data. All sites exhibit a much broader daily range of O3 concentration values than those observed at BBY. Even the smallest daily range observed at the rural Grass Valley site can easily double the typical daily range in MDA8 O3 found at BBY (Fig. 11a). This is expected as the much more rural BBY site is exposed to minimal urban emissions allowing for stratO3 to appear more prevalent at the surface.

An analysis of the lowest elevation surface monitoring site MDA8 O3 concentrations gives insight into the differences between coastal and inland sites of similar elevation and latitude. Elk Grove being the lowest elevation among all the sites at 7 m exhibits a substantially greater daily range of MDA8 O3 than that of BBY (Fig. 11c). This gives an indication of the impacts of high urban emissions at inland sites reacting with UV radiation in the formation and depletion of O3. The small daily range at BBY could indicate the importance of marine stratus clouds blocking the incoming solar radiation required for strong O3 formation and depletion.

d. Correlations among sites

A correlation analysis was performed utilizing the calculated surface MDA8 O3 values. The calculated correlation coefficients for the 15 sfcO3 monitoring stations for 25 July through 17 August 2016 are recorded in Table 2. Correlations for the MDA8 O3 concentrations between two surface sites were calculated based on an exact date and hour comparison. The strongest correlations between individual surface monitoring stations MDA8 O3 concentrations were found to be within the subregion height category: low, middle, or high (Table 2). It is important to note that while the correlations between the middle and low sites are all strong correlations, variations in correlation strength still occur. This shows the importance of latitude and longitude among the transport of urban emissions and other O3 precursors in the lower 110 m of the SAC air basin. The correlations among the high-elevation surface sites were weaker than those observed among the low and middle category sites.

Table 2.

Correlation coefficients for the calculated MDA8 O3 comparison of exact time and hour observations for 25 Jul–17 Aug 2016 at two given stations. The SAC sites are listed in order of lowest elevation to highest elevation above sea level. The bold values highlight the strongest correlation for each surface monitoring station.

Table 2.

Generally, as the distance between the two surface monitoring stations under comparison increases in the vertical and horizontal directions, the correlation becomes weaker. The Davis station located farthest west, the Elk Grove station located farthest south and lowest in elevation, and the Grass Valley station located farthest north and highest in elevation generally exhibited weaker correlations. Weak to little correlation was found between the calculated surface MDA8 O3 values for BBY and the SAC surface stations (Table 2).

The high-elevation surface sites display both positive and negative correlations with the BBY surface MDA8 O3 data (Table 2). The Colfax and the Cool sites exhibited very weak positive correlations with the BBY surface data, and stronger correlations with the SAC monitoring sites than did the other three high-elevation sites. The stronger correlations are likely due to the sites’ near-45° bearing from the heart of Sacramento. Summertime thermally driven upslope flows are known to transport pollutants from Sacramento to the northeast Sierra Nevada foothills (Fast et al. 2012). Therefore, these sites would not be strong candidates to further understand stratO3 transport. Three sites, Auburn, Placerville, and Grass Valley, each displayed a very weak, negative correlation with BBY surface data, indicating a height dependency on the O3 correlation. For completion, a correlation analysis was performed between all five high-elevation sites and elevated BBY ozonesonde measurements of similar elevation.

The correlation analysis was performed as follows: between the afternoon BBY ozonesonde concentration between 400 and 1000 m at 100-m increments and at 2000 m, and the observed 2100 UTC sfcO3 observation at the five high-elevation surface monitoring sites for the same date. This value represents the observation that is closest to the ozonesonde measurements obtained at 2100 UTC ±15 min to observe the well-known daily maximum sfcO3 concentration. The correlation coefficients are recorded in Table 3. The O3 correlations became stronger, and sites that previously exhibited a negative correlation now display a positive correlation (Table 3). Of the five sites, the Placerville station, located roughly 200 km west from the BBY coast, exhibited the strongest correlations with the elevated BBY ozonesonde data. Therefore, the Placerville O3 observations were picked for further analysis.

Table 3.

Correlation coefficients for high-elevation sfcO3 values observed for the 2100 UTC hour with elevated Bodega Bay 2100 UTC ozonesonde measurements. The italicized values denote the three strongest correlations observed, the bold highlight the strongest correlation for each surface monitoring station.

Table 3.

An analysis of sfcO3 data at Placerville and elevated BBY ozonesonde data shows the similarities between the locations. A clear variance with height is noticeable in the correlation strength between the Placerville sfcO3 data and BBY ozonesonde measurements, especially at similar elevations (Table 3). Three elevations exhibited a moderately strong correlation of 0.61 and a dependent/independent factor of 0.37 for the case study period, a visual to these relationships are given with a linear regression plot (Fig. 12). Figure 13 shows the change in O3 concentration and percentage from one afternoon to the next at the three elevations of interest and at Placerville. It can be inferred that the O3 at either location are often influenced by the same source region, yet the strength of the impact varies and appears more influential at the North Bay area coastal site than the Sierra Nevada foothill surface site (Fig. 13). Of the observed daily O3 changes, on 10 dates the 4 locales O3 variance were either all positive or negative. Three groups of interesting data emerged from these daily O3 variations, and the dates listed in Table 4 are further discussed.

Fig. 12.
Fig. 12.

Linear regression plot for elevated BBY observed O3 and Placerville 2100 UTC observed surface station O3 for the case study period 25 Jul–16 Aug 2016; dots are observations.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Fig. 13.
Fig. 13.

Daily observed ozone variations, in both changes in percentage (solid bar) and in concentration (hatched bar), for three elevated BBY locations ozonesonde observations (colors) and 2100 UTC Placerville sfcO3 observations (white); case study period 25 Jul–16 Aug.

Citation: Journal of Applied Meteorology and Climatology 58, 12; 10.1175/JAMC-D-18-0322.1

Table 4.

O3 observations and daily changes (Δ) in O3 concentration and percent from the date prior observed at the three elevated BBY points of interest and at the Placerville surface monitoring station during the dates of interest.

Table 4.

The first case emerged at the beginning of the period on 26 and 27 July. All sites exhibited an increase on 26 July, followed by a decrease on 27 July (Fig. 13). The daily afternoon O3 changes were similar in value, if not matching (Table 4). It can be inferred from Fig. 2a that the tropopause was low in the days prior. This likely resulted in stratO3 transport into the lower troposphere due to a rapid change in tropopause height (Hocking et al. 2007). Contributing to the case of stratospheric influence was high PV in the 0.5–1.0 km (Fig. 3). On 27 July, the observed BBY ozonesonde values approached 120 ppb at 2 km (Fig. 2b), as the Soberanes fire in Monterey County had another outbreak (Center for Atmospheric Research and Education 2016).

The second case of interest occurred from 3 to 4 August. The daily changes in O3 are the greatest of the period (Fig. 13). The observations on 2 August show an increase throughout most of the 1–5 km column, with a downward trend on 3 August and a large spike at 1 km, corresponding with the downward progression of a proposed low-level intrusion (Fig. 9a). During the launch on 3 August, the observed concentrations at 1 km reached 100 ppb (Fig. 2b). Though there are signs of stratospheric influence, these data were also subject to fire influences. The Cold Fire in Yolo County was active and located between Placerville and the BBY coast (Center for Atmospheric Research and Education 2016).

The strongest case for quantifying stratO3 transport into the lower 1 km was the final case, 11 August through 14 August, and corresponds with SI 3. There were no fire outbreaks or growth and the Cold Fire had been extinguished. The O3 variances at Placerville were very similar to that observed in the elevated BBY ozonesonde data. Figure 12 shows an observed increase in O3 at BBY 0.6–1.0 km and Placerville on 11 and 12 August, followed by a decrease in O3 at 1.0 km and Placerville on 13 August, and then a decrease in O3 at all levels on 14 August. Observations on 10 August show an increase in O3 at 1 km and Placerville, no change to 800-m O3, and a decrease in 600-m O3. Daily O3 variations at Placerville appear to follow more closely with the time fluctuations at 1 km; the daily O3 concentration changes were most like those observed at BBY 600 m. This analysis shows that the 0.6–1.0 km elevated region was influenced by 10–20 ppb of stratO3 per day as it progressed downward on 11–14 August 2016 above Northern California, at least during the afternoon peak O3 h (Table 4).

5. Conclusions

Stratospheric intrusions are known to be plentiful above the California region, especially along the North Pacific storm tracks. It is widely accepted that the observed values of O3 measured at western coastal sites are a good indication of bgO3 values due to the prevailing onshore flow. Therefore, the O3 concentrations measured at BBY show the temporal variability of bgO3 due to SI without strong anthropogenic influences. This study highlights that using 1.0 PVU is adequate to observe the deep penetration of stratospheric air masses into the lower troposphere above Northern California. The results show that high O3 incidences due to plausible deep SI effect coastal sfcO3 levels during the 2016 NH summer (e.g., from late July to early August) and likely influence sfcO3 levels in the SAC, and describes a likely synoptic setup that potentially brings stratospheric ozone influence to the lower troposphere in the California region of interest, likely influencing surface ozone concentrations directly.

This study identifies the downward vertical transport of O3 from the point of stratospheric injection to the surface at BBY. Other studies have similarly recognized transport of stratO3 to within the BL (e.g., Hocking et al. 2007; Tarasick et al. 2019). For this study, in regions of the stratO3 intrusion events, a downward progression of increasing O3 with time is distinct within the BBY ozonesonde daily percent change data. The positive increase in O3 was tracked downward, reaching the lowest 1 km of the ozonesonde profile and the surface. These O3 increases were noticeable in the overnight surface monitoring data from on site. This study also recognizes the similarities detected within the MERRA-2 values of PV for the vertical cross section including BBY and the SAC. It appears that the O3 measurements captured by the BBY ozonesonde give a good indication of O3 concentrations elevated high above the SAC. The greatest impacts of baseline O3 entering California above 2 km is within the elevated terrain of eastern California (Cooper et al. 2011). For this case the strongest spatial similarities exhibited were above 2 km mean sea level.

During this selected time frame, the SAC air quality proved to be moderate to harmful. However, the high-elevation surface sites often contributed to this nonattainment. Also, the reduced daily range of MDA8 O3 at the high-elevation sites indicates a greater influence of bgO3 than local O3 pollution in comparison to the lower-elevation sites. Although observed O3 concentrations were very similar when sites are in close proximity, the small difference shows that O3 is highly variable. This implies that correlations between observations of O3 concentrations at similar altitude over a greater distance would not be expected to be strong. A moderate correlation would indicate that air masses observed at two sites become regionally similar during events that cover a greater region simultaneously, such as during SI.

Elevated surface monitoring sites in the lower foothills of SAC can be separated into two categories. The first category includes sites where O3 observations are influenced by lower-elevation surface pollution. The Colfax monitoring site has a strong correlation with most of the SAC surface monitoring sites. The correlation found between the Colfax sfcO3 and the elevated BBY ozonesonde data remained weaker than that observed with the lower-elevation SAC site (Table 3). This further contributes to knowledge of surface pollution from the heart of Sacramento being transported northeasterly upslope to the Sierra Nevada foothills. The second category includes sites that are influenced by the O3 in an upper-level air mass. A height dependency correlation between BBY and high-surface-elevation sites in SAC shows a change from a weak negative correlation to a moderate positive correlation for three O3 monitoring sites; Grass Valley, Placerville, and Auburn. This shows that O3 concentrations observed at these surface sites were more closely related to mixing from the air above than below.

This study demonstrates that sfcO3 in Placerville and the air mass elevated above BBY were influenced similarly by stratO3 during a SI to the region of Northern California. A moderately strong correlation was found between the observed afternoon Placerville sfcO3 concentrations and the elevated BBY ozonesonde data at similar elevations. Observations between the three strongest correlated BBY elevated O3 and Placerville show that daily changes in O3 at all locations exhibited days where the O3 substantially increased, and a decrease the following day. The case of 11 August, the concentration changes under observation were near identical. The occurrence of this is suggestive of both locations simultaneously being influenced highly by bgO3 that is stratospheric in nature and can be considered a regional influence. Therefore, a closer study of the vertical column of O3 above both the BBY and SAC regions, during forecasted SIs in spring when events are most prevalent, via simultaneous ozonesonde launches would be beneficial.

While this study has merit in defining two locations that, if studied further, would lead to better estimations of stratO3 surface influence in Northern California and introduces a useful set of O3 data for future atmospheric and air quality modeling studies, it has limitations. The ozonesonde dataset was a contribution to the larger CABOTS 2016 air quality campaign. The NASA flights and NOAA ground-based lidar measurements took focus to the south in the San Joaquin Valley, and the deployment time of these platforms did not line up consistently with the time frame of this study. A similar campaign design with focus in SAC could lead to quantifying the direct influence of stratO3 contributing to the total sfcO3 pollution in the nonattainment zone.

Questions emerge about the linkage between high PV descending to the lower stratosphere and the timing of the wildfire influence on the region. While this study uses 3 different vertical cross sections for the analysis of the arrival of high PV into BBY, the picture is not complete. There were multiple probable lower-level stratO3 intrusions that occurred in correspondence with the upper-level enclosed lows that crossed through British Columbia and the Pacific Northwest prior to the period, and between SI 1 and SI 2. Further study into the exact location and timing of the wildfires could link dry stratospheric air, rich in O3, with the strength of a firestorm. Previous studies do suggest that fires are affected by SIs (Charney et al. 2003; Zimet et al. 2007; Langford et al. 2015). Future work will perform a trajectory analysis for the dates of interest, leading to answers of how often the air entering these locations crosses the same path, taking on influences of similar air masses.

Acknowledgments

We acknowledge the suppliers of datasets utilized in this research. We wish to express our appreciation to Drs. Jin Xue and Andy Langford for the suggestions for the development of this research. Proofreading by Dr. Ju-mee Ryoo was much appreciated. Comments and suggestions from three anonymous reviewers were highly appreciated. This research was supported by the NASA MUREP Grant NNX15AQ02A and the California Air Resources Board Contract 15RD007. The research is based on the thesis research of the first author and repeated in this paper with permission.

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  • Lin, M., A. M. Fiore, L. W. Horowitz, A. O. Langford, S. J. Oltmans, D. Tarasick, and H. E. Rieder, 2015: Climate variability modulates western US ozone air quality in spring via deep stratospheric intrusions. Nat. Commun., 6, 7105, https://doi.org/10.1038/ncomms8105.

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  • Liu, G., D. W. Tarasick, V. E. Fioletov, C. E. Sioris, and Y. J. Rochon, 2009: Ozone correlation lengths and measurement uncertainties from analysis of historical ozonesonde data in North America and Europe. J. Geophys. Res., 114, D04112, https://doi.org/10.1029/2008JD010576.

    • Search Google Scholar
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  • Oltmans, S. J., and Coauthors, 1996: Summer and spring ozone profiles over the North Atlantic from ozonesonde measurements. J. Geophys. Res., 101, 29 179–29 200, https://doi.org/10.1029/96JD01713.

    • Crossref
    • Search Google Scholar
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  • Oltmans, S. J., A. S. Lefohn, J. M. Harris, and D. S. Shadwick, 2008: Background ozone levels of air entering the west coast of the US and assessment of longer-term changes. Atmos. Environ., 42, 6020–6038, https://doi.org/10.1016/j.atmosenv.2008.03.034.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Parrish, D. D., K. C. Aikin, S. J. Oltmans, B. J. Johnson, M. Ives, and C. Sweeny, 2010: Impact of transported background ozone inflow on summertime air quality in a California ozone exceedance area. Atmos. Chem. Phys., 10, 10 093–10 109, https://doi.org/10.5194/acp-10-10093-2010.

    • Crossref
    • Search Google Scholar
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  • Roelofs, G. J., and Coauthors, 2003: Intercomparison of tropospheric ozone models: Ozone transport in a complex tropopause folding event. J. Geophys. Res., 108, 8529, https://doi.org/10.1029/2003JD003462.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Ryoo, J.-M., D. W. Waugh, and A. Gettelman, 2008: Variability of subtropical upper tropospheric humidity. Atmos. Chem. Phys., 8, 2643–2655, https://doi.org/10.5194/acp-8-2643-2008.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Ryoo, J.-M., M. S. Johnson, E. L. Yates, L. T. Iraci, R. B. Pierce, T. Tanaka, and W. Gore, 2017: Investigating sources of ozone over California using AJAX airborne measurements and models: Assessing the contribution from long-range transport. Atmos. Environ., 155, 53–67, https://doi.org/10.1016/j.atmosenv.2017.02.008.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Škerlak, B., M. Sprenger, and H. Wernli, 2014: A global climatology of stratosphere–troposphere exchange using the ERA-Interim data set from 1979 to 2011. Atmos. Chem. Phys., 14, 913–937, https://doi.org/10.5194/acp-14-913-2014.

    • Crossref
    • Search Google Scholar
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  • Stein, A. F., R. R. Draxler, G. D. Rolph, B. J. B. Stunder, M. D. Cohen, and F. Ngan, 2015: NOAA’s HYSPLIT atmospheric transport and dispersion modeling system. Bull. Amer. Meteor. Soc., 96, 2059–2077, https://doi.org/10.1175/BAMS-D-14-00110.1.

    • Crossref
    • Search Google Scholar
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  • Stevenson, D. S., and Coauthors, 2006: Multimodel ensemble simulations of present-day and near-future tropospheric ozone. J. Geophys. Res., 111, D08301, https://doi.org/10.1029/2005JD006338.

    • Search Google Scholar
    • Export Citation

  • Stohl, A., and Coauthors, 2003: Stratosphere-troposphere exchange: A review, and what we have learned from STACCATO. J. Geophys. Res., 108, 8516, https://doi.org/10.1029/2002JD002490.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Tarasick, D. W., and Coauthors, 2019: 2019: Quantifying stratosphere-troposphere transport of ozone using balloon-borne ozonesondes, radar windprofilers and trajectory models. Atmos. Environ., 198, 496–509, https://doi.org/10.1016/j.atmosenv.2018.10.040.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Trickl, T., H. Vogelmann, H. Giehl, H.-E. Scheel, M. Sprenger, and A. Stohl, 2014: How stratospheric are deep stratospheric intrusions? Atmos. Chem. Phys., 14, 9941–9961, https://doi.org/10.5194/acp-14-9941-2014.

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  • Waugh, D. W., 2005: Impact of potential vorticity intrusions on subtropical upper tropospheric humidity. J. Geophys. Res., 110, D11305, https://doi.org/10.1029/2004JD005664.

    • Crossref
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  • Wernli, H., and M. Bourqui, 2002: A Lagrangian “1-year climatology” of (deep) cross-tropopause exchange in the extratropical Northern Hemisphere. J. Geophys. Res., 107, 4021, https://doi.org/10.1029/2001JD000812.

    • Crossref
    • Search Google Scholar
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  • Zimet, T., J. E. Martin, and B. E. Potter, 2007: The influence of an upper-level frontal zone on the Mack Lake Wildfire environment. Meteor. Appl., 14, 131–147, https://doi.org/10.1002/met.14.

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  • Langford, A. O., K. C. Aikin, C. S. Eubank, and E. J. Williams, 2009: Stratospheric contribution to high surface ozone in Colorado during springtime. Geophys. Res. Lett., 36, L12801, https://doi.org/10.1029/2009GL038367.

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  • Lefohn, A. S., H. Wernli, D. Shadwick, S. J. Oltmans, and M. Shapiro, 2012: Quantifying the importance of stratospheric- tropospheric transport on surface ozone concentrations at high- and low-elevation monitoring sites in the United States. Atmos. Environ., 62, 646–656, https://doi.org/10.1016/j.atmosenv.2012.09.004.

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  • Lin, M., and Coauthors, 2012: Springtime high surface ozone events over the western United States: Quantifying the role of stratospheric intrusions. J. Geophys. Res., 117, D00V22, https://doi.org/10.1029/2012JD018151.

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  • Lin, M., A. M. Fiore, L. W. Horowitz, A. O. Langford, S. J. Oltmans, D. Tarasick, and H. E. Rieder, 2015: Climate variability modulates western US ozone air quality in spring via deep stratospheric intrusions. Nat. Commun., 6, 7105, https://doi.org/10.1038/ncomms8105.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Liu, G., D. W. Tarasick, V. E. Fioletov, C. E. Sioris, and Y. J. Rochon, 2009: Ozone correlation lengths and measurement uncertainties from analysis of historical ozonesonde data in North America and Europe. J. Geophys. Res., 114, D04112, https://doi.org/10.1029/2008JD010576.

    • Search Google Scholar
    • Export Citation

  • Oltmans, S. J., and Coauthors, 1996: Summer and spring ozone profiles over the North Atlantic from ozonesonde measurements. J. Geophys. Res., 101, 29 179–29 200, https://doi.org/10.1029/96JD01713.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Oltmans, S. J., A. S. Lefohn, J. M. Harris, and D. S. Shadwick, 2008: Background ozone levels of air entering the west coast of the US and assessment of longer-term changes. Atmos. Environ., 42, 6020–6038, https://doi.org/10.1016/j.atmosenv.2008.03.034.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Parrish, D. D., K. C. Aikin, S. J. Oltmans, B. J. Johnson, M. Ives, and C. Sweeny, 2010: Impact of transported background ozone inflow on summertime air quality in a California ozone exceedance area. Atmos. Chem. Phys., 10, 10 093–10 109, https://doi.org/10.5194/acp-10-10093-2010.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Roelofs, G. J., and Coauthors, 2003: Intercomparison of tropospheric ozone models: Ozone transport in a complex tropopause folding event. J. Geophys. Res., 108, 8529, https://doi.org/10.1029/2003JD003462.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Ryoo, J.-M., D. W. Waugh, and A. Gettelman, 2008: Variability of subtropical upper tropospheric humidity. Atmos. Chem. Phys., 8, 2643–2655, https://doi.org/10.5194/acp-8-2643-2008.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Ryoo, J.-M., M. S. Johnson, E. L. Yates, L. T. Iraci, R. B. Pierce, T. Tanaka, and W. Gore, 2017: Investigating sources of ozone over California using AJAX airborne measurements and models: Assessing the contribution from long-range transport. Atmos. Environ., 155, 53–67, https://doi.org/10.1016/j.atmosenv.2017.02.008.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Škerlak, B., M. Sprenger, and H. Wernli, 2014: A global climatology of stratosphere–troposphere exchange using the ERA-Interim data set from 1979 to 2011. Atmos. Chem. Phys., 14, 913–937, https://doi.org/10.5194/acp-14-913-2014.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Stein, A. F., R. R. Draxler, G. D. Rolph, B. J. B. Stunder, M. D. Cohen, and F. Ngan, 2015: NOAA’s HYSPLIT atmospheric transport and dispersion modeling system. Bull. Amer. Meteor. Soc., 96, 2059–2077, https://doi.org/10.1175/BAMS-D-14-00110.1.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Stevenson, D. S., and Coauthors, 2006: Multimodel ensemble simulations of present-day and near-future tropospheric ozone. J. Geophys. Res., 111, D08301, https://doi.org/10.1029/2005JD006338.

    • Search Google Scholar
    • Export Citation

  • Stohl, A., and Coauthors, 2003: Stratosphere-troposphere exchange: A review, and what we have learned from STACCATO. J. Geophys. Res., 108, 8516, https://doi.org/10.1029/2002JD002490.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Tarasick, D. W., and Coauthors, 2019: 2019: Quantifying stratosphere-troposphere transport of ozone using balloon-borne ozonesondes, radar windprofilers and trajectory models. Atmos. Environ., 198, 496–509, https://doi.org/10.1016/j.atmosenv.2018.10.040.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Trickl, T., H. Vogelmann, H. Giehl, H.-E. Scheel, M. Sprenger, and A. Stohl, 2014: How stratospheric are deep stratospheric intrusions? Atmos. Chem. Phys., 14, 9941–9961, https://doi.org/10.5194/acp-14-9941-2014.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Waugh, D. W., 2005: Impact of potential vorticity intrusions on subtropical upper tropospheric humidity. J. Geophys. Res., 110, D11305, https://doi.org/10.1029/2004JD005664.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Wernli, H., and M. Bourqui, 2002: A Lagrangian “1-year climatology” of (deep) cross-tropopause exchange in the extratropical Northern Hemisphere. J. Geophys. Res., 107, 4021, https://doi.org/10.1029/2001JD000812.

    • Crossref
    • Search Google Scholar
    • Export Citation

  • Zimet, T., J. E. Martin, and B. E. Potter, 2007: The influence of an upper-level frontal zone on the Mack Lake Wildfire environment. Meteor. Appl., 14, 131–147, https://doi.org/10.1002/met.14.

    • Crossref
    • Search Google Scholar
    • Export Citation
  • <sc>Fig</sc>. 1.
    View in gallery
    Fig. 1.

    (a) Location of the 15 surface ozone monitoring stations across Northern California and the Bodega Bay ozonesonde launch site. (b) 3D layout of the Sacramento surface stations with location names.

  • <sc>Fig</sc>. 2.
    View in gallery
    Fig. 2.

    Bodega Bay near-daily ozonesonde observations. Color scale concentrations from 0 to 160 ppb. (a) all CABOTS data, 2016. (b) 25 Jul–16 Aug 2016.

  • <sc>Fig</sc>. 3.
    View in gallery
    Fig. 3.

    MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections for (left) 26 Jul, (middle) 27 Jul, and (right) 28 Jul 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.

  • <sc>Fig</sc>. 4.
    View in gallery
    Fig. 4.

    MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections on (left 4 Aug, (middle) 5 Aug, and (right) 6 Aug 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.

  • <sc>Fig</sc>. 5.
    View in gallery
    Fig. 5.

    MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections on (left) 9 Aug, (middle) 10 Aug, and (right) 11 Aug 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.

  • <sc>Fig</sc>. 6.
    View in gallery
    Fig. 6.

    NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 27 Jul 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.

  • <sc>Fig</sc>. 7.
    View in gallery
    Fig. 7.

    NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 5 Aug 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.

  • <sc>Fig</sc>. 8.
    View in gallery
    Fig. 8.

    NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 9 Aug 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.

  • <sc>Fig</sc>. 9.
    View in gallery
    Fig. 9.

    (a) Calculated percent change in O3 from the BBY afternoon ozonesonde 100-m average values from day to day, increases in O3 for SI 1 and plausible low-level intrusions (P) are marked where a, b, and c specify which cross sections indicate high PV to the region, 26 Jul–4 Aug. (b) Calculated percent change in O3 from the BBY afternoon ozonesonde 100-m average values from day to day, increases in O3 for SI 2 and SI 3 with plausible low-level intrusion (P3) are marked where a, b, and c specify which cross sections indicate high PV to the region, 4–14 Aug.

  • <sc>Fig</sc>. 10.
    View in gallery
    Fig. 10.

    (a) Classic boxplot for the calculated maximum daily 8-h average ozone at BBY for 25 Jul–17 Aug 2016, local hour 0 through 23, orange bar = daily mean, black bar = daily median. (b) Onsite min-by-min BBY sfcO3 observations 30 Jul–4 Aug. (c) Onsite min-by-min BBY sfcO3 observations 10–15 Aug. Green boxes indicate dates and times that the stratO3 is suggested to have influenced the sfcO3 concentrations based on the ozonesonde analysis.

  • <sc>Fig</sc>. 11.
    View in gallery
    Fig. 11.

    Calculated surface MDA8 O3 concentration boxplots for 25 Jul–17 Aug 2016 for the SAC and BBY: (a) high-, (b) mid-, (c) low-elevation surface sites; colored bar = daily mean, black bar = daily median.

  • <sc>Fig</sc>. 12.
    View in gallery
    Fig. 12.

    Linear regression plot for elevated BBY observed O3 and Placerville 2100 UTC observed surface station O3 for the case study period 25 Jul–16 Aug 2016; dots are observations.

  • <sc>Fig</sc>. 13.
    View in gallery
    Fig. 13.

    Daily observed ozone variations, in both changes in percentage (solid bar) and in concentration (hatched bar), for three elevated BBY locations ozonesonde observations (colors) and 2100 UTC Placerville sfcO3 observations (white); case study period 25 Jul–16 Aug.

Fig. 1.

(a) Location of the 15 surface ozone monitoring stations across Northern California and the Bodega Bay ozonesonde launch site. (b) 3D layout of the Sacramento surface stations with location names.
Fig. 2.

Bodega Bay near-daily ozonesonde observations. Color scale concentrations from 0 to 160 ppb. (a) all CABOTS data, 2016. (b) 25 Jul–16 Aug 2016.
Fig. 3.

MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections for (left) 26 Jul, (middle) 27 Jul, and (right) 28 Jul 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.
Fig. 4.

MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections on (left 4 Aug, (middle) 5 Aug, and (right) 6 Aug 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.
Fig. 5.

MERRA-2 2100 UTC PV and wind speed reanalysis data along three vertical cross sections on (left) 9 Aug, (middle) 10 Aug, and (right) 11 Aug 2016, color plotted open contours for values of 1.0, 1.5, 2.0, and 5.0 PVU, gray filled contours of wind speed; and 250 hPa geopotential height contours and wind speed in the upper-left corners. (a) NW to SE, (b) SW to NE, and (c) W to E.
Fig. 6.

NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 27 Jul 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.
Fig. 7.

NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 5 Aug 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.
Fig. 8.

NOAA HYSPLIT isentropic 96-h ensemble back trajectories for 2100 UTC 9 Aug 2016 at multiple elevations in the vertical column elevated above the BBY ozonesonde launch site.
Fig. 9.

(a) Calculated percent change in O3 from the BBY afternoon ozonesonde 100-m average values from day to day, increases in O3 for SI 1 and plausible low-level intrusions (P) are marked where a, b, and c specify which cross sections indicate high PV to the region, 26 Jul–4 Aug. (b) Calculated percent change in O3 from the BBY afternoon ozonesonde 100-m average values from day to day, increases in O3 for SI 2 and SI 3 with plausible low-level intrusion (P3) are marked where a, b, and c specify which cross sections indicate high PV to the region, 4–14 Aug.
Fig. 10.

(a) Classic boxplot for the calculated maximum daily 8-h average ozone at BBY for 25 Jul–17 Aug 2016, local hour 0 through 23, orange bar = daily mean, black bar = daily median. (b) Onsite min-by-min BBY sfcO3 observations 30 Jul–4 Aug. (c) Onsite min-by-min BBY sfcO3 observations 10–15 Aug. Green boxes indicate dates and times that the stratO3 is suggested to have influenced the sfcO3 concentrations based on the ozonesonde analysis.
Fig. 11.

Calculated surface MDA8 O3 concentration boxplots for 25 Jul–17 Aug 2016 for the SAC and BBY: (a) high-, (b) mid-, (c) low-elevation surface sites; colored bar = daily mean, black bar = daily median.
Fig. 12.

Linear regression plot for elevated BBY observed O3 and Placerville 2100 UTC observed surface station O3 for the case study period 25 Jul–16 Aug 2016; dots are observations.
Fig. 13.

Daily observed ozone variations, in both changes in percentage (solid bar) and in concentration (hatched bar), for three elevated BBY locations ozonesonde observations (colors) and 2100 UTC Placerville sfcO3 observations (white); case study period 25 Jul–16 Aug.
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