A double peak in the seasonality of California's photosynthesis as observed from space
Solar-induced chlorophyll fluorescence (SIF) has been shown to be a powerful proxy for photosynthesis and gross primary productivity (GPP). The recently launched TROPOspheric Monitoring Instrument (TROPOMI) features the required spectral resolution and signal-to-noise ratio to retrieve SIF from space. Here, we present a downscaling method to obtain 500 m spatial resolution SIF over California. We report daily values based on a 14 d window. TROPOMI SIF data show a strong correspondence with daily GPP estimates at AmeriFlux sites across multiple ecosystems in California. We find a linear relationship between SIF and GPP that is largely invariant across ecosystems with an intercept that is not significantly different from zero. Measurements of SIF from TROPOMI agree with MODerate Resolution Imaging Spectroradiometer (MODIS) vegetation indices – the normalized difference vegetation index (NDVI), enhanced vegetation index (EVI), and near-infrared reflectance of vegetation index (NIRv) – at annual timescales but indicate different temporal dynamics at monthly and daily timescales. TROPOMI SIF data show a double peak in the seasonality of photosynthesis, a feature that is not present in the MODIS vegetation indices. The different seasonality in the vegetation indices may be due to a clear-sky bias in the vegetation indices, whereas previous work has shown SIF to have a low sensitivity to clouds and to detect the downregulation of photosynthesis even when plants appear green. We further decompose the spatiotemporal patterns in the SIF data based on land cover. The double peak in the seasonality of California's photosynthesis is due to two processes that are out of phase: grasses, chaparral, and oak savanna ecosystems show an April maximum, while evergreen forests peak in June. An empirical orthogonal function (EOF) analysis corroborates the phase offset and spatial patterns driving the double peak. The EOF analysis further indicates that two spatiotemporal patterns explain 84 % of the variability in the SIF data. Results shown here are promising for obtaining global GPP at sub-kilometer spatial scales and identifying the processes driving carbon uptake.
Photosynthesis is the process by which plants and other organisms use sunlight to synthesize carbon dioxide (CO2) and water to glucose and oxygen. Accurate knowledge of gross primary productivity (GPP) through photosynthesis is crucial for understanding the land–atmosphere carbon exchange, which is one of the largest and most uncertain aspects of the global carbon cycle (IPCC, 2013; Anav et al., 2015; USGCRP, 2018). This uncertainty in the land–atmosphere carbon exchange has led to long-standing questions regarding the magnitude of the Northern Hemispheric terrestrial carbon sink and how it has changed over the past few decades (e.g., Tans et al., 1990; Ballantyne et al., 2012; Ciais et al., 2019). As such, methods of inferring GPP are of great interest to the scientific community.
Previous work estimating regional or global-scale GPP has typically relied on biosphere models (e.g., the early work on SiB2 from Sellers et al., 1986), used remote-sensing measurements in Monteith light-use efficiency models with scalings for different ecosystems and climatic conditions (e.g., Monteith, 1972; Mahadevan et al., 2008), or attempted to back out GPP from CO2 flux inversions (e.g., CarbonTracker from Peters et al., 2007). The advent of global remote-sensing observations of solar-induced chlorophyll fluorescence (SIF) represents a breakthrough in our ability to constrain photosynthetic activity from space. This is because a number of studies have shown SIF to be a powerful proxy for photosynthesis both in laboratory environments (e.g., Baker, 2008) and at larger spatial scales (e.g., Frankenberg et al., 2011a; Parazoo et al., 2014; Yang et al., 2015, 2017; Y. Sun et al., 2017, 2018; Magney et al., 2019a). During the initial stage of photosynthesis, absorbed sunlight excites chlorophyll a molecules. The primary pathways for de-excitation are via photochemistry or non-photochemical quenching, the latter of which dissipates excess energy as heat when the plant does not have the capacity for photosynthesis (i.e., under stress). However, a small fraction dissipates as heat or is re-emitted as fluorescence and can be measured by remote sensing. This remote-sensing retrieval is termed SIF.
The first global space-borne measurements of SIF were made by Frankenberg et al. (2011b) and Joiner et al. (2011) using observations from the Japanese Greenhouse Gases Observing Satellite (GOSAT) instrument (Kuze et al., 2009). Since then, SIF has been retrieved from other space-borne instruments such as the Global Ozone Monitoring Experiment-2 (GOME-2) on the MetOp-A satellite, Scanning Imaging Absorption Spectrometer for Atmospheric Chartography (SCIAMACHY) on the Envisat satellite, the Orbiting Carbon Observatory-2 (OCO-2) satellite, and TROPOspheric Monitoring Instrument (TROPOMI) on the Sentinel-5 Precursor satellite (Frankenberg et al., 2011a, b, 2012, 2014; Joiner et al., 2011, 2012, 2013, 2014, 2016; Guanter et al., 2012, 2015; Köhler et al., 2015, 2018). A number of upcoming satellite missions such as FLEX (Drusch et al., 2017) and TEMPO (Zoogman et al., 2017) will also measure SIF at higher spatial and temporal resolution. Efforts are underway to create a multi-decadal SIF record using different space-borne instruments (Parazoo et al., 2019), and a few groups have utilized machine learning techniques to create spatially continuous SIF datasets at 0.05∘ × 0.05∘ resolution (Zhang et al., 2018; Yu et al., 2019; Li and Xiao, 2019). Mohammed et al. (2019) presents a detailed review of different remote-sensing techniques for retrieving SIF from space-borne measurements.
Some work has shown SIF to be a better measure of carbon uptake than other vegetation indices that look at canopy “greenness”. This is, in part, because indices like the normalized difference vegetation index (NDVI) are a measure of photosynthetic capacity (Sellers, 1985), whereas SIF is a measure of the photosynthetic activity and is coupled to the radiation regime. For example, Luus et al. (2017) showed that the seasonal cycle of a biosphere model driven by SIF agreed with measurements of CO2, whereas the seasonal cycle from the model driven by the enhanced vegetation index (EVI) was markedly different from the CO2 observations. Joiner et al. (2011) showed that the seasonal cycles of SIF and EVI agree in some regions but not others. Walther et al. (2016) showed a decoupling of the photosynthesis and greenness dynamics in boreal evergreen forests by comparing SIF and EVI to model estimates of GPP, with SIF better capturing the seasonality of both deciduous broadleaf and evergreen needleleaf forests. Again, this is likely due to SIF capturing photosynthetic activity rather than photosynthetic capacity. More recently, Magney et al. (2019a) demonstrated a mechanistic link between SIF and GPP over the course of a year in a winter-dormant Northern Hemisphere conifer forest, despite retaining chlorophyll through the winter. Magney et al. (2019a) highlighted the potential for new satellite measurements of SIF from TROPOMI and OCO-2 to track GPP at coarse spatial resolution (3.5×7 km2).
Here, we present an oversampling and downscaling method to obtain daily estimates of SIF at 500 m resolution. To our knowledge, this is the highest resolution SIF dataset from satellite measurements. We then compare this downscaled 500 m SIF data to AmeriFlux sites across the state of California to assess the relationship between SIF and GPP. We finish by decomposing California's spatiotemporal patterns of photosynthesis and carbon uptake into the dominant modes using empirical orthogonal functions (EOFs). Here, we focus on California because there are a number of eddy flux towers and it encompasses a range of diverse ecosystems including deciduous and evergreen forests, irrigated croplands, and grasslands (see Fig. 1).
2.1 Satellite measurements of SIF from TROPOMI
TROPOMI (Veefkind et al., 2012) is a nadir-viewing imaging spectrometer with bands in the UV, visible, near-infrared, and shortwave infrared aboard the Sentinel-5 Precursor satellite. The Sentinel-5 Precursor satellite was launched into low Earth orbit on 13 October 2017 with an equatorial crossing time of 13:30 local solar time (LST) and a 16 d orbit cycle. TROPOMI has a wide swath (2600 km across track), enabling near-daily global coverage. The spatial resolution of the ground pixels is 7 km along track1 and 3.5–15 km across track (3.5 km at nadir and 15 km at the edge of the swath). Of particular relevance here is the near-infrared band (725–775 nm) that covers the far-red part of SIF emission and contains a number of solar absorption features in the solar irradiance (Fraunhofer lines), allowing for retrieval of SIF through the change in optical depth of Fraunhofer lines. Guanter et al. (2015) showed the potential for TROPOMI to retrieve SIF and Köhler et al. (2018) presented the first retrievals. Specifically, Köhler et al. (2018) used a 743–758 nm retrieval window that is devoid of atmospheric absorption features. TROPOMI has a spectral resolution of ∼0.4 nm and a signal-to-noise ratio of ∼2500 in this retrieval window. The TROPOMI SIF retrieval uses a singular value decomposition to derive the spectral basis functions from TROPOMI data over vegetation-free areas (e.g., oceans, ice, and deserts).
One particularly attractive feature of space-borne SIF retrievals is the low sensitivity to atmospheric scattering by aerosols and clouds. Specifically, Frankenberg et al. (2012) showed that 80 % of the emitted SIF could be retrieved in the presence of clouds with low-to-moderate optical thickness. As such, Köhler et al. (2018) filtered out pixels with cloud fractions larger than 80 % based on Visible Infrared Imaging Radiometer Suite (VIIRS) observations; we use this same cloud filtering here. This weak sensitivity to clouds is in contrast to reflectance-based measures of vegetation (e.g., NDVI) that can only be made in clear-sky conditions, potentially inducing a clear-sky bias in reflectance-based vegetation indices.
Here, we apply one additional bias correction to the TROPOMI retrievals that was not included in Köhler et al. (2018). We find some mostly barren regions have systematically negative SIF values, which is non-physical. This bias is thought to be related to bright surfaces and is likely due to the choice of training data for the spectral basis functions. We are investigating ways to correct this globally. In the interim, we compute a spatiotemporal bias correction (where i,j are the spatial coordinates and k is the temporal coordinate) such that the mean SIF for a given location over a 30 d moving window is always positive. That is to say,
where is the 1-month block average for the kth day at location i,j. This still allows for negative SIF values due to variability and noise but will shift the mean SIF for a given 500 m grid cell to be positive. In practice, this bias correction is small, with 78 % having no bias correction at all and 90 % of the grid cells having a bias correction smaller than 0.1 mW m−2 sr−1 nm−1. The bias correction primarily impacts desert regions in southeastern California (see Fig. S1 in the Supplement).
2.2 Satellite-based vegetation indices from MODIS
The MODerate Resolution Imaging Spectroradiometer (MODIS) is an imaging spectrometer on NASA's Terra and Aqua satellites. Terra was launched in 2000 and Aqua was launched in 2002; both are in Sun-synchronous orbits with 16 orbits per day. Terra and Aqua have equatorial crossing times at 10:30 and 12:00 LST, respectively. Schaaf et al. (2002) developed the nadir bidirectional reflectance distribution function-adjusted reflectance (NBAR) dataset, hereafter referred to as the MODIS NBAR dataset. MODIS data over a 16 d period from Terra and Aqua can be combined to build a 500 m composite: MCD43A4. Here, we use the MCD43A4.006 (v06) MODIS NBAR dataset to compute three MODIS vegetation indices at 500 m resolution. Specifically, we compute the NDVI, EVI, and near-infrared reflectance of vegetation index (NIRv):
where ρNIR, ρred, and ρBlue are the reflectances in their respective MODIS bands, and G, C1, C2, and L are coefficients for the MODIS EVI algorithm (L=1, C1=6, and C2=7.5, G=2.5).
2.3 GPP estimates from AmeriFlux eddy covariance sites
AmeriFlux is a network of long-term eddy covariance sites that launched in 1996 (Baldocchi et al., 2001). These eddy covariance sites provide a direct measure of net ecosystem exchange (NEE; CO2 fluxes) (Baldocchi et al., 1988) and can be used to evaluate both bottom-up models and satellite proxies of carbon exchange. Disentangling the CO2 fluxes into GPP (CO2 uptake) and total ecosystem respiration (Reco; CO2 released) generally requires making assumptions about the temperature dependence of the respiration which can induce biases in the GPP estimate (Reichstein et al., 2005). Nevertheless, these eddy covariance sites provide the best estimate of site-level GPP across multiple ecosystems in California including croplands, wetlands, woody savannas, and grasslands. Here, we use data from 11 AmeriFlux sites across California (see Table 1) to evaluate the SIF retrievals from TROPOMI. NEE flux partitioning at these sites was performed using artificial neural networks from nighttime measurements to constrain Reco (Hemes et al., 2019).
a Vegetation classification is based on the International Geosphere-Biosphere Programme (IGBP) classification scheme (Strahler et al., 1999). b CRO (croplands) are lands covered with temporary crops followed by harvest and a bare soil period (e.g., single and multiple cropping systems). Note that perennial woody crops will be classified as the appropriate forest or shrub land cover type. c WET (permanent wetlands) are lands with a permanent mixture of water and herbaceous or woody vegetation that cover extensive areas. The vegetation can be present in either saltwater, brackish water, or freshwater. d GRA (grasslands) are lands with herbaceous types of cover. Tree and shrub cover is less than 10 %. e WSA (woody savannas) are lands with herbaceous and other understory systems, and with forest canopy cover between 30 % and 60 %. The forest cover height exceeds 2 m.
2.4 Comparison of TROPOMI SIF with MODIS vegetation indices
Figure 2 shows a scatterplot comparison of TROPOMI SIF and MODIS NDVI, EVI, and NIRv. The comparison is limited to coincident observations between March and August (MAMJJA) and excludes scenes that are predominantly barren or shrubland. A few features that immediately stand out are as follows:
There is a strong correspondence between EVI and NIRv. We find a nearly linear relationship between these two indices (r2=0.98).
All three MODIS indices are well correlated with each other (r2>0.85). We do observe a weakly non-linear relationship between NIRv and EVI or NDVI (see the curvature in the NIRv row).
There is a weaker relationship between SIF and the vegetation indices. Previous work has argued that NIRv is strongly correlated with SIF (Badgley et al., 2017) and provides a new independent approach for estimating GPP (Badgley et al., 2019).
Of the three vegetation indices examined here, we find the strongest relationship between NIRv and SIF, but it only explains half of the variability on daily timescales (r2=0.52). The agreement improves at coarser temporal scales (annual r2 = 0.83–0.84 and monthly r2 = 0.59±0.23). It is important to note that the native spatial resolution of the TROPOMI observations is 3.5 km across track at nadir, whereas the MODIS observations are 500 m across track at nadir. As such, we are using all MODIS observations within a single TROPOMI scene. Comparison of four methods of downscaling SIF with NIRv yields coefficients of determination of r2 = 0.52–0.64; see Fig. S2).
As mentioned above, the nominal spatial resolution of the ground pixels from TROPOMI is 3.5×7 km2 at nadir. However, the wide swath from TROPOMI (2600 km across track) often results in multiple observations per day (see Fig. 3b). Additionally, the orientation of these swaths differs over the 16 d orbit cycle, allowing us to infer higher spatial resolution than the nominal spatial resolution. This idea has been widely used with the space-borne OMI instrument that preceded TROPOMI (see K. Sun et al., 2018, and references therein for a discussion of oversampling with OMI observations). However, the spatial resolution of TROPOMI is a factor of 15 finer than OMI (3.5×7 km2 for TROPOMI and 14×26 km2 for OMI, both at nadir). Oversampling with OMI often required years of observations (e.g., Zhu et al., 2014). The wide swath and dense spatial coverage of TROPOMI allow us to perform biweekly oversampling.
Figure 3 shows a schematic of how the oversampling is performed. Figure 3a shows two hypothetical swaths from TROPOMI overlaid on a 500 m grid (same spatial resolution as the MODIS NBAR dataset). Areas where the swaths overlap allow us to partition the information down to a finer spatial scale. For example, the yellow pixel in swath B overlaps with all four pixels from swath A. As such, the signal from that pixel in swath B can be subdivided to finer spatial scales. Each unique shade of color would correspond to unique information in Fig. 3a. Figure 3b shows the sampling density of TROPOMI over California on a single day in June 2018; the dark blue region indicates where two TROPOMI swaths overlapped that day.
We find that, on average, each 500 m grid cell is within the bounds of ∼0.6 TROPOMI scenes with a successful retrieval per day. By using biweekly oversampling (a moving 14 d window), we obtain approximately eight different swath orientations over a 14 d period for the oversampling. These eight swath orientations allow us to further refine our grid to follow the schematic shown in Fig. 3. It also means that the daily values presented here are representative of 14 d moving averages (centered about that day).
We can take the oversampling a step further by pre-weighting the SIF signal in a TROPOMI scene by the underlying vegetation fraction; we refer to this as “downscaling”. That is to say, we assume the observed SIF from TROPOMI in a given scene likely originates from more vegetated regions within that scene. Here, we use a relative weighting for this downscaling:
where s⋆ is the retrieved SIF from TROPOMI for a single scene, si,j is the SIF spatially downscaled to 500 m, vi,j is the vegetation indices from MODIS that fall within the bounds of a single scene from TROPOMI (i.e., the gray boxes within a TROPOMI box in the left panel of Fig. 3), and is the mean vegetation index over a given TROPOMI scene. Using Eq. (5) with returns the unweighted oversampling result. Following this, si,j will naturally revert to oversampling in regions with homogeneous vegetation (as inferred by MODIS).
Figure 4 shows the 2018 annual mean SIF from TROPOMI from Köhler et al. (2018) at 0.05∘ × 0.05∘ spatial resolution and California's seasonal cycle at weekly temporal resolution (non-bias corrected). The middle and bottom rows of Fig. 4 show the 2018 annual mean SIF and seasonal cycle using oversampling and spatially downscaled with NIRv from MODIS. All three show consistent large-scale spatial patterns. We do, however, find significant differences between the results from Köhler et al. (2018) and the oversampling or downscaling method over the San Francisco Bay Area where the complex topography induces numerical artifacts such as high SIF values over water. We also point out that the Köhler et al. (2018) seasonal cycle is produced at weekly temporal frequency, whereas we produce daily estimates using a 14 d moving window. The oversampling and downscaling methods both yield consistent large-scale patterns and seasonal cycles (left panels in Fig. 4). The main impact of the MODIS-based local downscaling is a sharpening effect. This can be seen in the right column of Fig. 4. Importantly, the gradients observed in the oversampled SIF are also present in the downscaled SIF. The choice of which MODIS vegetation index to use in the downscaling makes little difference, as the r2 between the different downscaled SIF products ranges from 0.99 to 1.00 (see Fig. S2); hereafter, we use SIF downscaled with NIRv because, of the three vegetation indices, NIRv showed the strongest correlation to SIF (see Fig. 2). Again, we stress that the large-scale spatiotemporal patterns are conserved between the oversampling and downscaling methods, and the nuanced difference in processing allows for analysis at much finer spatiotemporal scales. That is to say that we are not inducing large-scale changes in the spatiotemporal patterns with these different methods of processing; those are robustly driven by the underlying SIF retrievals.
Previous work has shown strong empirical relationships between SIF and GPP at coarse spatial scales (e.g., Walther et al., 2016; Jeong et al., 2017; Parazoo et al., 2018; Zuromski et al., 2018; Y. Sun et al., 2018). Magney et al. (2019a) recently extended this SIF–GPP relationship by showing, in a conifer forest, how both SIF and GPP are regulated by seasonal changes in photoprotective pigments and how SIF is directly related to needle physiology.
Lee et al. (2013), Guanter et al. (2014), and Y. Sun et al. (2017) have previously argued for a linear relationship between SIF and GPP; this follows from a simple relational analysis. From Monteith theory (Monteith, 1972), we can write
where is the light-use efficiency of CO2 assimilation, I is the photosynthetically active radiation (PAR), and α is the fractional absorbance of PAR. An analogous expression can be written for SIF (Lee et al., 2013):
where ΦF is the light-use efficiency of SIF and β is the probability of SIF photons escaping the canopy. Rearranging yields
From Eq. (8), we can see that GPP should be proportional to SIF. However, there are likely differences in between ecosystems. Notably, Yang et al. (2018) argued that SIF is more strongly correlated with the absorbed PAR (αI) than with GPP at subdaily timescales, which implicitly points to non-linearities in . β will be a function of the canopy structure and likely differs between ecosystems, although some studies have argued that reflectance measurements could be used to infer β (Yang and van der Tol, 2018; Zeng et al., 2019). Additionally, the ratio of to ΦF will likely be ecosystem specific due to, for example, differences in photosynthetic pathways (C3 versus C4 plants; Liu et al., 2017). A number of studies have found the relationship between chlorophyll fluorescence and GPP to be non-linear at the leaf scale (e.g., Magney et al., 2017, 2019b), owing the increased linearity at the canopy scale to averaging SIF and GPP over many different leaf angles exposed to highly heterogenous light environments.
Figure 5 compares the TROPOMI SIF retrievals to observations from AmeriFlux sites across California (see Table 1 and Fig. 1 for the locations). The gray dots in Fig. 5 are all of the AmeriFlux GPP estimates and the black dots are those between 13:00 and 14:00 PST, similar to the TROPOMI overpass time (equatorial overpass time is 13:30 LST at nadir). This overpass time is fortuitous in that it generally coincides with the daily maximum in GPP at the AmeriFlux sites. The green dots are the actual TROPOMI SIF retrievals at that location that have the scene-specific relative weighting from the MODIS NIRv (Eq. 5). No temporal smoothing has been applied in Fig. 5. We find a strong correspondence between SIF and GPP across four different ecosystems. The top left panel shows that SIF clearly captures the onset of photosynthesis as well as the punctuated seasonal cycle of GPP in a corn field (US-Bi2) with r2=0.79. We also observe the gradual increase in GPP and abrupt decline at a woody savanna site (US-Ton) and grassland site (US-Var) with r2 = 0.40 and r2=0.59, respectively. The relatively high variability in SIF at US-Ton and US-Var from July to December (1σ spread of 0.33 mW m−2 sr−1 nm−1) contrasts the low variability during the dormant period at US-Bi2 and is likely associated with bright surfaces (implying a higher retrieval uncertainty), quantifying the upper range of anticipatable noise. The bottom row of Fig. 5 shows a comparison of TROPOMI SIF with GPP from three different wetland sites on Twitchell Island in the Sacramento–San Joaquin River Delta; we generally find a strong correspondence between TROPOMI SIF and the three wetland sites (r2=0.42, 0.42, and 0.30 for US-Tw1, US-Tw4, and US-Tw5). The inter-site differences in GPP within a single ecosystem are larger than the SIF–GPP differences, indicating some fine-scale heterogeneity that is likely not being captured here. In any case, the reasonable agreement with the GPP at the wetland sites is encouraging because standing water can often bias reflectance-based indices, particularly in the NIR (Gamon et al., 2013).
From this SIF–GPP comparison in Fig. 5, we infer a SIF–GPP scaling factor of 18.5±4.9 [(µmol m−2 s−1) (mW m−2 sr−1 nm−1)−1] across the six sites in Fig. 5 (range of scaling factors is 13–25; see Fig. S3). Our comparison of TROPOMI SIF with GPP from AmeriFlux sites in California indicates larger inter-ecosystem differences in the SIF–GPP relationship than intra-ecosystem differences, lending credence to this universal scaling factor. However, there are two important caveats: (1) we do not have an eddy covariance site in an evergreen forest, which is a major limitation, as much of California is dominated by evergreen forests, and (2) we are not directly measuring GPP with SIF. As such, we refer to this SIF-estimated GPP as
This single scaling from Eq. (9) seems to be a reasonable relation given the available information, with the caveat that there could be differences between ecosystems that are unaccounted for. To reiterate, there is a clear correspondence between the observed SIF and GPP estimated for the different AmeriFlux sites (see Fig. 5) but we have a limited number of AmeriFlux sites in California that do not cover all ecosystems. As such, we do not report GPP here and have included an asterisk to highlight the caveats with the relationship presented here. Future work to obtain a more robust SIF–GPP relationship covering more ecosystems is warranted.
Figure 6a shows the SIF-derived seasonal cycle of photosynthesis in California. One of the most prominent features is the apparent double peak in the seasonal cycle. This double peak is present in both 2018 and 2019 with similar timing of the maxima. The first peak occurs in April and the second peak occurs in June. Interestingly, the trough between these peaks occurs near the annual maximum in PAR (red line in Fig. 6d). This begs the following question: what is driving this double peak in the seasonality of California's photosynthesis?
We can use the CropScape database (see Fig. 1) to determine the ecosystems driving the spatiotemporal patterns in the TROPOMI SIF data, as it provides land cover classifications across the state of California at 30 m spatial resolution. However, a notable limitation of the classifications from the CropScape data is the lack of discrimination for non-cropland areas. For example, grasslands and pastures are combined into a single land type that seems to also include regions that would typically be defined as oak savanna and chaparral. In lieu of a better sub-kilometer land cover dataset, we use the classifications from the CropScape database for this work.
Figure 6a shows a breakdown of the regions contributing to the statewide SIF signal based on the land cover data from the CropScape database. We find the California grasslands and pastures (a single classification that also includes chaparral and oak savanna) have a single peak that coincides with the first statewide peak in April; this is consistent with the seasonal cycle at California grassland sites in the AmeriFlux network (Fig. 5) that show a unimodal peak in the spring that ends in May. Figure 6e and e′ show the mean spatial pattern in April 2018 and 2019, respectively, where we see that the April peak coincides with a statewide increase in SIF. There are a few pertinent hotspots in grasslands or pastures during this April peak. Notably, California's Central Valley and surrounding hills exhibit a strong photosynthesis signal in April. The valley to the east of Bodega Bay (38.3∘ N, 122.9∘ W) appears as a large hotspot in both 2018 and 2019. This region lies on transect B in Fig. 1, and the seasonal cycle is shown in more detail in Fig. 7.
The second peak in June shows a dominant contribution from evergreen forests (Fig. 6a). This can also be seen in the spatial patterns from Fig. 6f and f′ where the evergreen forests in Northern California exhibit a strong SIF signal. California's Central Valley can be clearly distinguished, as the surrounding hills have dried out (predominantly oak savanna and chaparral). The observed photosynthesis from the Central Valley is maintained by heavily irrigated cropland throughout the valley.
The yellow line in Fig. 6b indicates the fraction of SIF in California that comes from cropland. We see the largest relative contribution occurring in the fall. However, this is primarily because all other ecosystems have gone dormant (see Fig. 6g) as opposed to an increase in photosynthetic activity from cropland. The only region that shows an increase in photosynthesis is the rice fields in the Sacramento Valley (the valley surrounding Sutter Buttes at 39.1∘ N, 121.5∘ W) in Northern California. The rice fields show a SIF signal in excess of 2.5 mW m−2 sr−1 nm−1 during the fall (GPP∗ in excess of 45 µmol m−2 s−1).
Both 2018 and 2019 show a double peak in the seasonal cycle; however, the onset of the grassland-driven peak differs substantially between the two years. This difference is likely driven by the increased precipitation in 2019 (blue line in Fig. 6d). There was 50 % more precipitation in 2019 compared to 2018, and the precipitation occurred earlier in the water year. By mid-February 2019, there was more precipitation than the annual total from 2018. This early precipitation allowed for an earlier and longer growing season for the grasses. Figure 8 shows the difference in spatial patterns between 2019 and 2018. In general, we find reasonable consistency between the two years in April and June but substantial differences in the fall. We find a factor of 2 increase in statewide SIF between fall 2018 and 2019. This increase from 2018 to 2019 is exhibited across all ecosystems. This is, again, likely due to the increased precipitation in 2019 compared to 2018. The MODIS vegetation indices show negligible differences between fall 2019 and 2018 (see Figs. S6 and S7). Most of the major differences in April and June are due to ecosystem disturbances such as fires. The 2018 Northern California fires are a striking example of that (three large negative anomalies in Fig. 8b); the impact of these fires is currently the focus of forthcoming work. An additional feature that stands out is the positive SIF anomaly in Southern California; this increase in 2019 is due to the low rainfall the previous year.
Interestingly, none of the MODIS vegetation indices (NDVI, EVI, or NIRv) show this double peak in photosynthesis (Fig. 6c). The seasonal cycles from the three vegetation indices show a greening that starts in mid-winter (begins in December 2018) and increases roughly linearly to a peak in April. All three vegetation indices maintain that peak until July when they show a roughly linear decline through the fall. The seasonal cycle of the three MODIS vegetation indices bears a strong similarity to the clear-sky PAR seasonal cycle. This difference between SIF and the MODIS vegetation indices may be due to a clear-sky bias, as the reflectance-based vegetation indices (NDVI, EVI, and NIRv) can only be made under clear-sky conditions, whereas SIF can be retrieved in the presence of some clouds and aerosols (Frankenberg et al., 2011b). This is inferred by the decline in PAR during May 2018 and May 2019 (Fig. 6d) that corresponds to a decline in SIF. This highlights one of the differences between SIF and the MODIS vegetation indices: the vegetation indices are reflectance-based products, whereas SIF is a fluorescence signal emitted during photosynthesis and is thus coupled to the radiation regime. This again gets back to the idea that SIF is measuring photosynthetic activity, whereas the MODIS indices are measuring photosynthetic capacity.
Several ecophysiological reasons could also explain the SIF detection of a double peak feature, whereas MODIS vegetation indices do not. Nearly 11 % of the state of California consists of the California oak savanna (many in the foothills of coastal mountains and the Sierras; Tyler et al., 2006). Over the course of the season, these ecosystems operate as an evergreen ecosystem, whereby understory grass is photosynthetically active during the winter months, while trees (primarily oak species) reach extremely high values of maximum carboxylation capacity (Vcmax) during the spring when water is plentiful, and then retain their leaves throughout the summer in a highly photoprotective state (i.e., US-Ton; Xu and Baldocchi, 2003). Spatially, we observe increased SIF values in oak savanna as well as chaparral ecosystems (also present on coastal and Sierra foothills) in the early spring when available soil moisture is at a maximum (Xu and Baldocchi, 2004; Xu et al., 2004). As these ecosystems enter the hot, dry summers, increases in sustained non-photochemical quenching and decreases in photochemistry result in decreased fluorescence while still appearing “green” to MODIS vegetation indices. Meanwhile, snow is melting rapidly at higher elevations, making water available for many of the needleleaf evergreen species in the Sierras and coastal ranges; then the water resources become depleted and temperatures cool, prompting these evergreen species to go back into a photoprotective state, resulting in a short, photosynthetically active growing season that has been shown to be more well characterized by SIF from GOME-2 than MODIS NDVI and EVI (Zuromski et al., 2018). Future work comparing SIF and MODIS indices with measured PAR at AmeriFlux sites would be useful in further evaluating the role of radiation and physiology in the double peak feature.
Figure 7 shows a Hovmöller diagram for two transects across Northern California (see Fig. 1 for the location of the transects). Transect A in Fig. 7 shows the short but strong SIF signal from the rice fields. The timing of the SIF signal from the rice fields agrees with the growing cycle for rice in California. Rice in the Sacramento Valley is typically planted in mid-to-late May; the fields are then flooded and harvested in mid-to-late September (University of California at Davis, 2018). This observation of the rice fields is encouraging because we are observing photosynthesis in the presence of standing water, which can often bias reflectance-based indices in the NIR (Gamon et al., 2013). In both 2018 and 2019, we observe the onset of photosynthesis at the rice fields in the first few days of June and a rapid decline at the end of September. Transect B begins in the valley to the east of Bodega Bay (location of the grassland hotspot) and crosses the Central Valley. This grassland hotspot is present from April through May of both 2018 and 2019. The valley near Bodega Bay is dominated by pastures; however, it is currently unclear why this particular region exhibits a stronger SIF signal than other pastures in California. The persistent strong signal in 2018 and 2019 might make it an interesting site for study with an eddy covariance site in the future.
Section 5 discussed the spatiotemporal patterns for different regions and ecosystems; here, we present an alternative method of characterizing the dominant modes of spatiotemporal variability in photosynthesis using EOFs and their associated principal components (PCs). EOFs are a matrix factorization that are commonly used to identify structure in a spatial dataset and yield a finite number of modes. These modes compactly represent the data and are often interpreted as physical modes of the system.
Figure 9 shows the first two EOFs and their associated PCs for the TROPOMI SIF data over California; the corresponding eigenvalue spectrum can be seen in Fig. S5. The first two EOFs corroborate the findings from Sect. 5 and, taken together, explain 84 % of the variability in the TROPOMI SIF data:
EOF 1: the mean signal and
EOF 2: the double peak.
The first EOF (Fig. 9a) represents the mean signal and explains 74 % of the variability in the TROPOMI SIF data. From the spatial pattern, we can see that it includes most of the biomass in California and is strongly correlated to the statewide mean SIF: r2=0.99. The associated principal component bears a strong similarity to the statewide mean SIF seasonal cycle (Fig. 6a). This finding is not entirely surprising because we are using unnormalized SIF data for the matrix factorization. This means that the most important mode of variability is the mean signal and that the following EOFs are anomalies relative to the mean signal.
The second EOF (Fig. 9b) represents the double peak in the timing of California's photosynthesis. This EOF combines the signal from the grasslands (positive phase of EOF 2) and the evergreen forests (negative phase of EOF 2). We find EOF 2 to be positively correlated with the grassland fraction from the CropScape database (r=0.55) and negatively correlated with the evergreen forests (). There is also a negative correlation with the rice fields (). The associated principle component serves to amplify the seasonal cycle from EOF 1 in grasslands during April and amplify the forest peak in June. This is because the red region (grasslands) in Fig. 9b will contribute a positive anomaly in April and a negative anomaly in June. Conversely, the blue region (evergreen forests and rice) will contribute a negative anomaly in April and a positive anomaly in June. This EOF arises because the grasslands and forests are both spatially separated and out of phase with each other, allowing the matrix factorization to place them into a single EOF that represents the processes driving the double peak in the timing of California's photosynthesis.
It should be noted that the EOF patterns found here are unlikely to be true “physical modes” (see, for example, Monahan et al., 2009). That is to say, we would not necessarily expect the response to a perturbation to follow patterns shown in Fig. 9. EOF 2 is a good example of this because it seems unlikely that the grasslands and forests will exhibit opposing responses to a forcing. Grasslands and forests are combined into a single EOF simply because there is little loss of information by combining them due to the spatial separation and phase offset. This is not to argue against the utility of EOFs. EOFs are a useful method for identifying structure in geophysical datasets, as evidenced here by their identification of the double peak in the timing of California's photosynthesis.
We present an oversampling and downscaling method to produce daily estimates of SIF, a proxy for photosynthetic activity, at 500 m spatial resolution from TROPOMI. To our knowledge, this is the highest spatial resolution SIF dataset from satellite measurements. We find a double peak in the seasonality of photosynthesis in California during 2018 and 2019, a feature that is not present in the MODIS vegetation indices (NDVI, EVI, or NIRv). Analysis of the spatial and temporal patterns of the SIF data indicates that the double peak is due to two ecosystems that are out of phase with each other: woody grasslands (e.g., grasslands, chaparral, and oak savanna) and evergreen forests.
Our work applies methods developed for previous satellite retrievals (oversampling) and uses estimates of subgrid-scale vegetation (downscaling) to produce daily 500 m spatial resolution SIF from TROPOMI over California. We use a 14 d moving window to produce this estimate. The oversampling method results in a smooth spatial field and removes artifacts due to complex topography and the wide TROPOMI swath. The downscaling method further refines the high-resolution spatial patterns by bringing in a priori information on the subgrid vegetation patterns. The oversampling and downscaling methods do not alter the large-scale spatiotemporal patterns, as they conserve the SIF signal over a single scene.
TROPOMI SIF data and MODIS vegetation indices are reasonably consistent at annual timescales over California but show weaker relationships at daily and monthly timescales. This implies that TROPOMI SIF is providing some information that is distinct from the MODIS vegetation indices. TROPOMI SIF data show a strong correspondence with half-hourly estimates of GPP at multiple AmeriFlux sites across different ecosystems including cropland, grassland, savanna, and wetlands. We find a linear relationship between SIF and GPP that is largely invariant across ecosystems with an intercept that is not significantly different from zero. As such, we use SIF as an estimate of GPP∗ with the caveat that some ecosystems are not represented in our California analysis.
The double peak in the seasonality of California's photosynthesis observed by TROPOMI SIF is due to two ecosystems that are out of phase with each other: grasses show a maximum in April and evergreen forests peak in June. An EOF analysis corroborates the phase offset and spatial patterns driving the double peak. The EOF analysis also indicates that two spatiotemporal patterns explain 84 % of the variability in the TROPOMI SIF data.
The results shown here are promising for obtaining global near-daily GPP at sub-kilometer spatial scales using satellite measurements. This, in turn, may prove helpful in addressing long-standing questions regarding the mechanisms and locations driving carbon uptake in the Northern Hemisphere. It would also allow us to monitor climate change impacts on vulnerable ecosystems at local to global scales.
The supplement related to this article is available online at: https://doi.org/10.5194/bg-17-405-2020-supplement.
AJT designed the research and conceived the methods. PK performed the satellite retrievals. AJT, PK, TSM, CF, IF, and RCC analyzed data. AJT wrote the paper; PK, TSM, CF, IF, and RCC provided comments on the paper.
The authors declare that they have no conflict of interest.
Alexander J. Turner is supported as a Miller Fellow with the Miller Institute for Basic Research in Science at UC Berkeley. Ronald C. Cohen acknowledges support from the TEMPO project SV3-83019. Philipp Köhler and Christian Frankenberg are funded by the Earth Science US participating investigator (grant no. NNX15AH95G). This research used the Savio computational cluster resource provided by the Berkeley Research Computing program at the University of California, Berkeley (supported by the UC Berkeley Chancellor, Vice Chancellor for Research, and Chief Information Officer). This research also used resources from the National Energy Research Scientific Computing Center, which is supported by the Office of Science of the US Department of Energy under contract no. DE-AC02-05CH11231. TROPOMI SIF and MODIS NBAR data are publicly available at ftp://fluo.gps.caltech.edu/data/tropomi/ (last access: 2 January 2020) and https://e4ftl01.cr.usgs.gov/MOTA/MCD43A4.006/ (last access: 2 January 2020), respectively. Funding for AmeriFlux data resources was provided by the US Department of Energy's Office of Science. We would like to thank Dennis Baldocchi (UC Berkeley) for sharing the AmeriFlux data and for providing extensive feedback on the work. Finally, we are extremely grateful to the team that has realized the TROPOMI instrument, consisting of the partnership between Airbus Defence and Space, KNMI, SRON, and TNO, commissioned by NSO and ESA.
This research has been supported by the Adolph C. and Mary Sprague Miller Institute for Basic Research in Science at the University of California Berkeley, the NASA TEMPO project (grant no. SV3-8019), and the NASA Earth Science participating investigator (grant no. NNX15AH95G).
This paper was edited by Martin De Kauwe and reviewed by Luis Guanter and one anonymous referee.
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