Galveston Bay and Coastal Ocean Optical-Geochemical Response to Hurricane Harvey From VIIRS Ocean Color.

Dissolved and particulate organic carbon, suspended particulate matter concentrations, and their optical proxies colored dissolved organic matter absorption and backscattering coefficients were studied in Galveston Bay, Texas, following the extreme flooding of Houston and surrounding areas due to Hurricane Harvey (25-29 August 2017) using field and ocean color observations. A three-step empirical-semianalytic algorithm for determination of colored dissolved organic matter absorption and backscattering coefficients revealed the dynamics of dissolved organic carbon and particle distribution from Visible and Infrared Imaging Radiometric Suite ocean color. Environmental drivers, especially floodwater discharge and winds, strongly influenced the spatiotemporal distribution of dissolved/particulate material in the bay and shelf waters following the hurricane passage. Over 10 days during/following the hurricane, ~25.2 × 106 kg C of total organic carbon and ~314.7 × 106 kg of suspended particulate matter were rapidly exported from Galveston Bay (representing ~0.65% and 0.27% of respective annual Mississippi River fluxes to the Gulf of Mexico), with potential for ecological impacts to shelf waters.

Introduction

Hurricane Harvey, after making landfall on the Texas coast as a category 4 hurricane on 25 August 2017, meandered inland, stalled, and deposited unprecedented rainfall that caused widespread flooding in the highly industrialized Houston Metropolitan and surrounding areas (>500 mm with return period >2,000 years under current climate and ~100 years by century end; Emmanuel, 2017) with potential for adverse ecological impacts due to elevated levels of dissolved and particulate organic matter (DOC and POC) and suspended particulate matter (SPM) in the floodwaters discharging into Galveston Bay. Thus, ability to monitor DOC, POC, and SPM or their optical proxies, chromophoric dissolved organic matter (CDOM), and scattering properties could provide insights into the bay's water quality and its distribution and transport into the coastal ocean following episodic events such as Hurricane Harvey, one of the most destructive hurricanes on record. Although field observations have generally provided a good understanding of the bay's geochemical properties (S. Lee et al., 2011; Wen et al., 2008), these are spatiotemporally limited, especially during extreme weather events. Satellite ocean color with its synoptic and near daily coverage has provided critical insights on the ocean's optical and biogeochemical response following hurricanes (D'Sa et al., 2010; Farfan et al., 2014; Lin et al., 2003; Lohrenz et al., 2008) but have been limited in the optically complex estuaries due to poor performance of the standard ocean color algorithms.

Empirical ocean color algorithms developed for many estuarine and coastal waters use remote sensing reflectance R (λ) band ratios (e.g., green to red bands) to relate to optical or geochemical quantities such as CDOM, SPM, or phytoplankton chlorophyll (Del Castillo & Miller, 2008; D'Sa et al., 2006, 2007; D'Sa & Miller, 2003; Joshi et al., 2017; Joshi & D'Sa, 2015; Le et al., 2013; Mannino et al., 2014; Tehrani et al., 2013) and are often optimized for a particular estuary or season based on the dominant constituents influencing the absorption properties. In contrast, semianalytic algorithms which relate satellite‐derived R (λ) to inherent optical properties (e.g., absorption a and backscattering b ) through relationships such as R  ≅ b /(a  + b ) provide a more generalized approach to retrieve the absorption and scattering properties of seawater (Z. Lee et al., 2002; Zhu et al., 2011). For instance, absorption a , a dominant source of variability in water leaving radiance, is composed of contributions by water itself (a ), phytoplankton (a phy), CDOM (a ), and nonalgal particulate matter (NAP; detrital and mineralogical particles; a NAP) and can be expressed as a  = a  + a phy + a  + a NAP, for wavelengths across the light spectrum. Variations in these constituent absorption properties have been mainly used to retrieve a phy or combined a  + a NAP (a ), as spectral shapes of CDOM and NAP absorption are similar and difficult to disentangle (Z. Lee et al., 2002). While these semianalytic relationships have been mainly developed for oceanic and coastal waters, more recently, a semianalytic approach has been proposed for estuaries and optimized for the Visible and Infrared Imaging Radiometric Suite (VIIRS) sensor (Joshi & D'Sa, 2018).

In this study, we present results of two field sampling surveys in Galveston Bay conducted approximately 1 and 2 months following Hurricane Harvey as part of a NASA Rapid Response project to assess the hurricane impact on the bay's water quality and bio‐optical state. Satellite estimates of CDOM (a 412) and NAP (a NAP 412) absorption coefficients at 412 nm and backscattering coefficient (b 532) at 532 nm were obtained from VIIRS using a combination of a new empirical and an estuarine tuned semianalytic algorithm (Quasi‐Analytical Algorithm for VIIRS [QAA‐V]; Joshi & D'Sa, 2018); then, using a series of cloud‐free imagery from before and after the hurricane, the environmental drivers on a 412 and b 532 distribution were examined. Finally, in situ hydrodynamic data (tides, currents, and river discharge) and satellite estimates of SPM, DOC, and POC concentrations at the bay entrance were used to determine export fluxes of these constituents to the coastal ocean during and immediately following Hurricane Harvey.

Data and Methods

Study Site and Field Sampling

Galveston Bay, a wide and shallow estuary (~2‐m average depth; 1,600‐km2 area) located along the upper coast of Texas (Figure 1a) is the seventh largest estuary in the continental United States. Major sources of freshwater to the estuary are the Trinity River (TR, ~50%), the San Jacinto River (SJR, ~30%), and local watersheds surrounding Galveston Bay (~20%; Guthrie et al., 2012; Lucena & Lee, 2017). The Houston Ship Channel is a deep (~14 m) and narrow channel connecting the bay to the northern Gulf of Mexico (GOM) through a narrow entrance, the Bolivar Roads Pass (Figure 1a). The bay region sampled in this study includes Trinity Bay (TB), Upper Galveston Bay (UGB), Lower Galveston Bay (LGB), and coastal stations near the bay entrance (Figures 1a and 3). Two field surveys were conducted on 29 September (survey1) and 29/30 October 2017 (survey2), respectively, following Hurricane Harvey. During both field surveys, surface water samples were collected along a transect from the riverine end‐member of the TR to the head of the estuary (Figure 1a; orange circles). Sampling at additional sites was conducted in the UGB and East Bay during survey2 (white circles).

Figure 1

(a) Galveston Bay with sampling stations occupied on 29 September and 29 October 2017 (orange circles) and additional stations on 30 October 2017 (white circles). (b) Discharge from the TR and the SJR. Relationships (c) between salinity and a 412 and between salinity and DOC, (d) between salinity and a NAP 412 and between salinity and SPM, (e) between a 412 and DOC, and (f) between a NAP 412 and SPM. TR = Trinity River; SJR = San Jacinto River; DOC = dissolved organic carbon; SPM = suspended particulate matter.

Figure 3

Sequence of VIIRS‐derived a 412 imagery of Galveston Bay and coast from before/after Hurricane Harvey. (bottom) mean satellite estimates of a 412 and DOC concentrations in the three subbays. VIIRS = Visible and Infrared Imaging Radiometric Suite; DOC = dissolved organic carbon; CDOM = colored dissolved organic matter; TB = Trinity Bay; UGB = Upper Galveston Bay; LGB = Lower Galveston Bay; EB = East Bay.

Optical and Geochemical Measurements

Surface water samples were filtered through 0.2‐μm prerinsed Nuclepore filters on the same day and stored in acid‐cleaned, precombusted amber bottles with Teflon‐lined caps at 4 °C in the dark and processed within a week for CDOM spectral absorption on a dual‐beam Perkin‐Elmer Lambda 850 spectrophotometer; the absorption coefficient at 412 nm (a 412) and spectral slope S between 275 and 295 nm were then determined (Joshi & D'Sa, 2015). Filtered samples were also processed for DOC on a Shimadzu total organic carbon analyzer (TOC‐5000A) using a high‐temperature combustion method (Benner & Strom, 1993; D'Sa et al., 2016). For determinations of light absorption by SPM, particles were collected onto 25‐mm‐diameter Whatman GF/F filter and stored in liquid nitrogen until measurement. Particulate (total and nonalgal) absorption were measured on a Perkin‐Elmer Lambda 850 spectrophotometer fitted with a 15‐cm‐diameter integrating sphere (Naik & D'Sa, 2012). SPM concentrations were determined by filtration through dry preweighed Whatman GF/F filters (Joshi & D'Sa, 2018; Neukermans et al., 2012). An optical package with a Wetlabs ecotriplet and a Sea‐Bird SBE conductivity‐temperature‐depth recorder was used to obtain measurements of chlorophyll and CDOM fluorescence, backscattering, and salinity at the sampling stations (D'Sa et al., 2006; Joshi & D'Sa, 2018). Above‐water measurements of water surface, sky, and reference plate radiances were collected using a GER 1500 512iHR spectroradiometer under clear‐sky conditions to obtain above‐water remote sensing reflectance (Rrs , sr−1) (Mobley, 1999; additional details in D'Sa & Miller, 2005; Joshi & D'Sa, 2018).

Ocean Color Satellite Data

VIIRS ocean color satellite data were obtained for clear‐sky days from the NASA Ocean Biology Processing Group website for days before and after Hurricane Harvey including two field surveys on 30 September (+1 day as compared to field survey) and 29 and 30 October 2017. Satellite data were processed using the NASA SeaDAS 7.4 software and corrected for the atmosphere using the MUMM NIR scheme (Ruddick et al., 2006). Satellite imagery were further processed using the QAA‐V to obtain estimates of b 532 and SPM (Joshi & D'Sa, 2018).

Hydrological, Meteorological, and Hydrodynamic Data

Discharge data were obtained from the U.S. Geological Survey gauge stations at Wallisville (~40 km from river mouth) for TR and the east and west fork stations for SJR (Figure 1b). Meteorological data (atmospheric pressure and winds) (Figure 2e) were obtained from a National Oceanic and Atmospheric Administration (NOAA) station at Eagle Point, Galveston. Hydrodynamic data (tides and currents) were obtained from the NOAA tides and currents (ADCP) station located at the entrance of Galveston Bay. Mean lower low water (MLLW) which is the National Ocean Service's nautical chart data and mean sea level (MSL) values which are available at hourly intervals were downloaded from NOAA's website. A 40‐hr low‐pass filter was used to remove the tidal variation (range < 0.5 m) from MSL. The difference between the local MSL and MLLW is the nontidal component or residual water level that is due to river flow and winds (Figure 2f). Near‐surface currents (speed and direction) were normalized along the bay entrance with current vectors shown above the water level line being directed out of the bay (e.g., ebb tide) while current vectors located below the water level line are directed into the bay (e.g., flood tide).

Figure 2

(a) Flowchart showing processing approach for obtaining VIIRS estimates of DOC and POC in Galveston Bay. Relationships between (b) band ratio R 551/R 671 (in situ and VIIRS derived) and in situ a 412 (a 412 + a NAP 412), (c) VIIRS‐derived (QAA‐V) and in situ b 532 and in situ a NAP 412, and (d) validation matchups of in situ and VIIRS‐derived a 412. Time series of (e) atmospheric pressure and winds and (f) water level and surface currents at Galveston Bay entrance. (g) Discharge from TR + SJR; volume water, DOC and POC fluxes through the Galveston Bay entrance (+/− into/out of the bay). Black arrows (e) indicate the wind vectors corresponding to VIIRS satellite imagery. VIIRS = Visible and Infrared Imaging Radiometric Suite; DOC = dissolved organic carbon; POC = particulate organic carbon; QAA‐V = Quasi‐Analytical Algorithm for VIIRS; TR = Trinity River; SJR = San Jacinto River; SPM = suspended particulate matter; NAP = nonalgal particulate matter; CDOM = colored dissolved organic matter.

Water Volume and Carbon Flux Calculations

The daily water volume flux (positive—inward; negative—outward; Figure 2g) through the Bolivar Roads Pass entrance was calculated by integrating the hourly flows across the bay entrance as follows: where the currents are directed inward (flood) or outward (ebb) of the bay (Figure 2f). The cross‐sectional area was calculated as the residual water level (detided MSL − MLLW) × width of the channel. DOC flux rates for days with cloud‐free VIIRS satellite imagery were computed by multiplying the mean satellite‐derived DOC concentration across the channel by the net volume of water transported through the pass (Joshi et al., 2017). DOC fluxes between 26 August and 4 September corresponding to high river discharge and water volume export (Figure 2g) were calculated by converting the daily water fluxes to daily DOC fluxes (based on a linear correlation between the two parameters) and then integrating the fluxes over the 10‐day period (similarly, for SPM and POC). DOC fluxes over a 1‐month period (26 August to 26 September 2017) were also estimated.

Results and Discussion

Hydrologic Conditions and Optical‐Geochemical Properties in Galveston Bay

River discharge was typical for SJR and TR (~1.52 and ~40.93 m3/s) for the month of August before Hurricane Harvey. However, for a short period during and after the hurricane passage, discharge peaked on 29 August for the eastern and western flanks of the SJR (3,367.70 and 3,707.30 m3/s) and for TR (1,035.28 m3/s) on 31 August. Discharge, however, dropped to low values for SJR by 4 September but remained elevated till mid‐September for TR, likely due to flooding over a larger drainage basin, to controlled water‐release from reservoirs and its passage through wetlands of the lower Trinity Basin (Figure 1b).

Although discharge from TR was typical for September (26.6 m3/s), salinity in Galveston Bay was lower during survey1 (2.00–21.25) than during survey2 (10.06–27.81) and generally lower than reported for the bay for the season (Han et al., 2006). DOC concentrations ranged from 852.4 to 394.84 μM C during survey1 and from 468.14 to 308.50 μM C during survey2, showing a general decrease with increasing salinity along the transect (Figure 1c). a 412 (the DOC optical proxy) ranged from 2.98 (near TR) to 1.24 m−1 (coastal station) during survey1 and 1.73 to 0.41 m−1 during survey 2, generally decreasing with increasing salinity (Figure 1c). Corresponding mean values of spectral slope S were 17.85 ± 0.34 μm−1 during survey1 and 20.11 ± 0.71 μm−1 during survey 2. High CDOM, low S, and high DOC during survey1 indicate strong terrestrial signature with little photodegradation of the dissolved organic matter pool compared to survey2. CDOM absorption has not been previously reported for the bay; however, mean values of a 412 (2.13 ± 0.52 m−1) during survey1 were relatively higher than previously reported for coastal and estuarine waters (D'Sa, 2008; Mannino et al., 2014; Tehrani et al., 2013). Overall, for the two surveys, DOC was significantly related to CDOM (Figure 1e) as follows: Similar relationships between DOC and CDOM absorption have been reported in other coastal and estuarine waters (Joshi et al., 2017; Tehrani et al., 2013). SPM was higher and more variable during survey1 (27.94 ± 12.36; min = 8.92, max = 53.50 mg/L) than during survey2 (18.49 ± 6.39; min = 6.8, max = 28.67 mg/L); overall it showed a decreasing trend with increasing salinity (Figure 1d). Similarly, a NAP 412, was also greater and more variable during survey1 (1.13 ± 0.48; min = 0.21, max = 2.11 m−1) than survey2 (0.90 ± 0.34; min = 0.24, max = 1.44 m−1) and showed decreasing trends with increasing salinity (Figure 1d). a NAP 412 values were greater than those previously reported for coastal waters of the northern GOM (D'Sa et al., 2007; Naik et al., 2011) and appeared to be well correlated to SPM in these turbid estuarine waters (Figure 1f). Particle (NAP plus phytoplankton) backscattering b 532 was also found to be well correlated to SPM in coastal waters including Galveston Bay (R 2 = 0.89; equation (16), Joshi & D'Sa, 2018), with a relationship given by Furthermore, a previously reported relationship between POC and SPM for Galveston Bay (Warnken & Santschi, 2004) was used to derive POC using the equation where POC* = POC/SPM. These relationships indicate a strong link between the optical and the geochemical properties. Furthermore, lower salinity and higher levels of DOC and SPM including their optical proxies during survey1 compared to earlier reported measurements strongly indicate longer‐term hurricane impact on the bay's geochemical properties.

VIIRS Estimates of CDOM/NAP Absorption and DOC/SPM/POC Concentrations

A comparison of in situ versus VIIRS‐derived Rrs revealed a good agreement for the green and red bands, compared to blue (Joshi & D'Sa, 2018, Table 4). Thus, using a green to red band ratio, the combined CDOM+NAP (a 412), followed by individual a NAP 412 and a 412 absorption coefficients, were obtained using the following steps (schematic, Figure 2a): (i) A Rrs551/Rrs671 band ratio (VIIRS and in situ) was observed to be highly correlated to a 412 with a power law equation (Figure 2b) given by (ii) b 532 was derived from VIIRS using an estuarine tuned semianalytic algorithm (QAA‐V; Joshi & D'Sa, 2018), (iii) a relationship between b 532 and a NAP 412 using both field and satellite observations (Figure 2c) was determined as This relationship was highly correlated and used to obtain estimates of a NAP 412 from VIIRS.

(iv) a 412 was then determined from the equation VIIRS‐derived a 412 was found to be well correlated to in situ a 412 (Figure 2d and supporting information Figure S1 show additional in situ validation of modeled/VIIRS‐derived parameters). DOC was then determined from VIIRS imagery using equation (2), while SPM was determined from b 532 (QAA‐V) using equation (3) (Joshi & D'Sa, 2018). Finally, POC was determined from SPM using equation (4).

Dissolved/Particulate Matter Distribution and Environmental Drivers

A series of cloud‐free VIIRS imagery obtained before and after Hurricane Harvey were used to assess a 412 and b 532 distributions (Figures 3 and 4), the optical proxies for DOC and SPM/POC, respectively. During this period, physical drivers such as river discharge, tides, and strong winds appear to have influenced the bay's optical‐geochemical properties (Figures 2e–2g, 3, and 4). About 1 month before Hurricane Harvey impacted the Texas coast, mean VIIRS‐derived surface a 412 (0.89 m−1) and b 532 (0.12 m−1) within the bay (Figures 3 and 4 and Table S1) were comparable to those reported in coastal waters of northern GOM (D'Sa, 2008; D'Sa et al., 2007); corresponding estimates of DOC (4.52 mg C/L), POC (1.34 mg C/L), and SPM (12.55 mg/L) were generally typical for the summer (Hung et al., 2001). However, 2 days after the hurricane passage (31 August), estimates of a 412 (6.29, 14.77, 8.67 m−1) and b 532 (1.01, 1.84, 2.97 m−1) increased to very high levels in TB, UGB, and LGB, respectively. Corresponding estimates of DOC (17.95, 39.06, and 23.88 mg C/L), POC (2.29, 2.64, and 2.77 mg C/L), and SPM (103.81, 190.52, and 220.51 mg/L; Figures 3 and 4 and Table S1) were some of the highest recorded, with estimates higher in UGB and LGB than TB, indicating stronger impact from SJR. Furthermore, a very coherent plume extending well offshore suggests the massive injection of DOC/POC/SPM‐laden freshwater tens of kilometers (~60 km on 31 August) into the shelf. Similar plumes of high CDOM/DOC and suspended particulate material into the shelf waters were observed from all the other bays and estuaries along the Texas‐Louisiana coast (Figures S2 and S3) suggesting that in aggregate, this event transported massive amount of terrestrial carbon and suspended sediments into the coastal ocean with potential for long‐term ecological impacts. Concentrations decreased significantly by 2 September (Figures 3 and 4 and Table S1), but high levels along the western bay indicated that the Houston Ship Channel formed an efficient conduit for transporting floodwaters discharged mainly through SJR into the coastal ocean due to its low residence time under high discharge conditions (Rayson et al., 2016).

Figure 4

Sequence of VIIRS‐derived b 532 imagery of Galveston Bay and coast from before/after Hurricane Harvey. (bottom) mean estimates of b 532 and POC concentrations in the three subbays. VIIRS = Visible and Infrared Imaging Radiometric Suite; POC = particulate organic carbon; TB = Trinity Bay; UGB = Upper Galveston Bay; LGB = Lower Galveston Bay; EB = East Bay.

By 7 and 8 September, concentrations of DOC, POC, and SPM were still elevated in comparison to 2 September, likely due to a cold front (strong northeasterly winds) related resuspension (Figure 2e). Satellite imagery revealed the dissipation of the plume and the westward advection of coastal waters (driven by strong northeasterly winds) with high CDOM and low NAP absorption (Figures S2 and S3). The origin of these coastal waters appears to be Sabine Lake (a high refractory DOC environment; Bianchi et al., 1997) whose drainage basin was also strongly impacted by Hurricane Harvey. The advection of coastal waters into the bay (e.g., Rayson et al., 2015) with relatively high CDOM/low particle waters (Figures 3 and 4) could have changed the bay's geochemical properties. While bay waters continued flowing into the shelf through 12 September as a strong plume, spatial patterns of optical properties through October indicated that (i) CDOM was the dominant absorption constituent, with elevated values persisting longer in the surrounding coastal waters (Figures S2 and S3); (ii) by 16 September, with discharge from SJR to prehurricane levels, floodwaters appeared to be flushed out of the western bay (low CDOM/particle scattering) but were elevated in the eastern bay, likely due to elevated discharge from TR and wetlands runoff and longer residence times of TB and East Bay (Rayson et al., 2016); (iii) while the hurricane resulted in longer‐term increases in DOC/POC/SPM, cold fronts appear to cause only short‐term increases in these constituents; and (iv) the fraction of organic content of particles (POC/SPM) decreased considerably from ~10.7% in July to ~1.3% during the 10‐day high river discharge period, subsequently increasing with time (Figure 4—bottom and Table S1) and generally consistent with earlier studies (e.g., Warnken & Santschi, 2004). In the shelf, DOC and SPM (Joshi & D'Sa, 2018) showed large along‐ and cross‐shelf variability influenced by plume strength, coastal currents, and frontal passages.

Dissolved/Particulate Matter Fluxes to the Coastal Ocean

The combined discharge from SJR and TR into the bay peaked (7,058.02 m3/s) on 28 August with dominant contribution from SJR (6,282.6 m3/s). Simultaneously, the volume water flux out of the bay increased steadily to a peak of ~4,146.5 m3/s on 28 August that coincided with a twofold increase in water level (1.11 ± 0.19 m above MLLW) and high outward surface currents (2.25 m/s) at the bay entrance (Figures 1b, 2f, and 2g) resulting in rapid flushing of floodwaters out of the bay and into offshore shelf waters as indicated by the imagery of 31 August (Figures 3 and 4). Overall, during and following the hurricane, the ebb tidal current (northeast) was generally much stronger than the flood tidal current (northwest; Figure 2f) due to the large volume of floodwaters in the bay. From a linear relationship observed between SPM and the river discharge (not shown) and assuming well‐mixed waters under strong flows, SPM export from the bay (mainly terrestrial material associated with floodwaters from SJR basin) between 26 August and 4 September was estimated at 314.7 × 106 kg (peak export of 163.8 × 106 kg on 29 August 2017), representing ~0.27% of the annual Mississippi River suspended sediment loading to the northern GOM (Meade & Moody, 2010). Estimates of DOC and POC exported to the shelf was 0.86 × 106 and 0.20 × 106 kg C on 31 August and 0.43 × 106 and 0.19 × 106 kg C on 2 September, respectively. DOC flux reduced to ~0.11 × 106 and 0.02 × 106 kg C on 7/8 September due to wind‐driven advection of coastal waters into the bay. DOC flux increased again on 12 September to 0.25 × 106 kg C. The integrated export of total organic flux (DOC plus POC) over a 10‐day period between 26 August and 4 September was 25.22 × 106 kg C (21.6 × 106 + 3.57 × 106 kg C), representing ~0.63% of the total annual organic flux by the Mississippi River to the northern GOM (4.0 × 109 kg C; Bianchi et al., 2007). The peak DOC flux export of 9.43 × 106 kg C on 29 August 2017 was in the range of the daily flux export of the Mississippi River (~8.49 × 106 kg/day; Bianchi et al., 2004; Del Castillo & Miller, 2008) or that exported by all the major estuaries to the mid‐Atlantic Bight over a 10‐day period (Mannino et al., 2015). Over the next 20 days (to 26 September), the total DOC flux exported out of Galveston Bay was estimated at 1.87 × 106 kg C, likely a contribution from the TR discharge and its greater residence time in TB (Grayson et al., 2016).

Conclusions

In this study, we used a combination of field and satellite ocean color observations to examine the impact of Hurricane Harvey on the bio‐optical and geochemical properties in Galveston Bay and surrounding coastal ocean. Field data indicated that even 1 month following the hurricane‐related flooding of the Texas coast, lower salinity prevailed over much of the bay with elevated levels of DOC and SPM concentrations. CDOM absorption and backscattering coefficients, the optical proxies for DOC, POC, and SPM, were estimated and validated from the VIIRS ocean color data using a combination of a new empirical and an estuarine tuned semianalytical algorithm. An analysis of a series of cloud‐free VIIRS imagery of CDOM absorption and backscattering revealed a highly dynamic response of the dissolved (DOC) and particulate matter (SPM/POC) constituents in different subregions of the bay. The differences in the river discharge patterns and residence times of freshwater in the bay, and meteorological events greatly influenced the transport and distribution of dissolved and particulate material in the bay and the coastal ocean. The massive initial pulse of discharge from SJR (equivalent to the low flow from the Mississippi River) and its rapid flow through the shipping channel into the coastal waters likely prevented its distribution in the bay. However, its transport with minimal transformation likely transferred massive amounts of material to the coastal waters with potential to strongly influence its water quality and ecosystem that warrants long‐term monitoring of the impacted coastal region. This study also demonstrates the application of novel ocean color algorithms for the relatively new VIIRS satellite sensor to elucidate the impact of extreme flooding on the dissolved and particulate matter dynamics in the coastal ocean.

Supporting Information S1

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