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2010 NORTHEASTERN NATURALIST 17(1):77–90
Impacts of Climate Change on Narragansett Bay
Leslie M. Smith1,*, Sandra Whitehouse2, and Candace A. Oviatt1
Abstract - The objective of this paper is to examine the impacts of global climate
change on Rhode Island’s coastal ecosystems. Average annual air temperature in
Rhode Island has increased by 1.7 °C since 1880, water temperatures of Narragansett
Bay have increased by 1.2 °C since 1950, precipitation increased 27% between
1895 and 1999, and sea level rose 0.13 m between 1931 and 2007. We can already
see the effects of these climatic changes on the Narragansett Bay ecosystem, including
ecological changes in the Bay’s food web from phytoplankton and zooplankton
to fish, e.g., changes in phenology of seasonal phytoplankton blooms and dominant
fish species (e.g., Pseudopleuronectes americanus [Winter Flounder]). These climatic
changes have increased freshwater inputs and the concomitant pollutant loads
into the Bay. Rising sea level has contributed to ongoing erosion of the coast and
has put waterfront homes at increased risk. It is imperative to continue monitoring
Compelling scientific evidence has shown that humans have been a key
driving factor in the dramatic changes we have seen in the earth’s climate
over the last 100 years. The fourth assessment report of the Intergovernmental
Panel on Climate Change (IPCC) has determined that it is very likely
(90% certainty) that anthropogenic emissions have contributed to global
climate change (IPCC 2007). The climate is changing faster than many ecosystems
can adapt, and the rate of change, rather than its magnitude, is the
key driver of the stress being placed on these ecosystems. Most forecasts
predict that the rate of change will increase over the coming decades.
Global air temperature has increased by 0.74 ± 0.18 °C over the last century
(IPCC 2007), while surface ocean temperatures (top 300 m) has increased
0.17 °C from 1955 to 2003 (Levitus et al. 2005). A disproportionate amount
of this surface ocean temperature change is centered on the North Atlantic
Ocean, which has increased at twice the rate as the global average over the
same time period (Levitus et al. 2005). Sea-level rise has accelerated in recent
years from the average rate of 1.8 mm per year from 1961–2003 to 3.1 mm per
year in 1993 to 2003 (IPCC 2007). The majority of the sea-level rise can be attributed
to thermal expansion (Meehl et al. 2007). An additional effect of the
increase in atmospheric concentration of CO2 is an increase in concentration
of dissolved CO2 in the oceans, which has lead to a decrease in pH from 8.25
to 8.14 over the 53 years from 1951 to 2004 (Jacobson 2005). The reduction of
pH in the oceans increases the dissolution rate of calcium carbonate (Caldeira
1Graduate School of Oceanography, University of Rhode Island, Box 9, 11 Aquarium
Road, Narragansett, RI 02882. 232 Elmgrove Avenue, Providence, RI 02906. *Corresponding
author - email@example.com.
78 Northeastern Naturalist Vol. 17, No. 1
and Wickett 2003, Feely et al. 2004, Orr et al. 2005) and raises the calcium carbonate
horizon, the level in the water column below which calcium carbonate
will dissolve (Doney 2006). These two factors threaten sensitive organisms
that use calcium carbonate in the production of their shells, e.g., pteropods,
foraminifera, corals, and some phytoplankton (Caldeira and Wickett 2003,
Feely et al. 2004, Orr et al. 2005)
Global climate change (GCC) is a worldwide phenomenon with consequences
not dispersed uniformly across the globe; consequently, different
areas will see different effects. Below we detail the patterns of global climate
change on Rhode Island’s coastal ecosystems, specifically Narragansett Bay,
with respect to changes in temperature, precipitation, storm intensity, sealevel
rise, and pH.
Rhode Island Impacts
Air temperature in Rhode Island has increased over the past century to
varying degrees depending on location and the types of instruments employed.
When data in the Historic Climate Network (HCN) are averaged,
they indicate that air temperature in Rhode Island increased 1.2 °C from
1895 to 1999 (New England Regional Assessment Group 2001). The same
raw data is utilized by the NASA Goddard Institute for Space Studies (GISS),
where it is adjusted for urbanization effects. The average of six long-term
GISS data sets from in and around Rhode Island indicate an air temperature
increase of 1.7 °C from 1881 to 2006 (Fig. 1). Data from the Providence and
T.F. Green Airport Weather Bureau sites shows an increase in air temperature
Figure 1. Air temperature in the Rhode Island region from 1881 to 2007. Data is collected
from six locations by the NASA Goddard Institute for Space Studies (GISS)
averaged by year. Locations and their time ranges include: Providence, RI (41.7N,
71.4W) 1881–2007; Worchester, MA (42.3N, 71.9W) 1949–2004; Kingston, RI
(41.5N, 71.5W) 1889–2007; Taunton, MA (41.9N, 71.1W) 1881–2007; Quonset
Point, RI (41.6N, 71.4W) 1945–1973; and Block Island, RI (441.2N, 71.6W) 1881–
1995. Data was accessed at http://data.giss.nasa.gov.
2010 L.M. Smith, S. Whitehouse, and C.A. Oviatt 79
from 1905 to 2006 of 0.9 °C (Pilson 2008). Global temperatures during
this same time period (1905 to 2006) have increased 0.74 ± 0.18 °C (IPCC
2007). New England regional temperatures have increased 0.4 °C between
1895 and 1999 (New England Regional Assessment Group 2001). In all
of these records, the cooling of air temperatures during the period of the
1950s through 1970s is evident and consistent with the global trend (IPCC
2007, New England Regional Assessment Group 2001). It appears that air
temperature in Rhode Island is increasing at a rate faster than the global or
New England regional averages, possibly the result of population growth
and urban expansion and/or the influence of the nearby warmer sea-surface
temperatures (New England Regional Assessment Group 2001).
Water temperature records show a similar trend to air temperature over
the past century. Long-term temperature datasets for water temperature in
Narragansett Bay come from observations collected by the National Oceanic
and Atmospheric Administration (NOAA) at the Newport Harbor tide gauge
(#8452660) from 1956 to 1999 (Hawk 1998, Nixon et al. 2004) and the University
of Rhode Island Graduate School of Oceanography’s (GSO) fish trawl
surveys collected at Fox Island in the lower West Passage of Narragansett Bay
since 1959 (Fig. 2; Collie et al. 2008). These datasets correspond well with the
122-year temperature record from Woods Hole, MA, about 60 km to the east
(Hawk 1998, Nixon et al. 2004) that shows annual temperatures in the 1990s
were 1.2 °C warmer than average annual temperatures from 1890 to 1970
(Nixon et al. 2004). It should be noted that water-temperature trends exhibited
the same cooling trends seen in air temperature from 1950–1970 (Nixon et al.
2004). Narragansett Bay water temperature has increased faster than the surface
(top 300 m) North Atlantic average, which warmed by 0.35 °C over the
Figure 2. Annual averages of weekly water-temperature measurements at Fox Island
in Narragansett Bay, Located in the lower West Passage of Narragansett Bay, show
an increase of 0.91 °C from 1959–2003 (0.021 °C/y). (Data was collected as part of
weekly GSO fish trawl survey).
80 Northeastern Naturalist Vol. 17, No. 1
past century (Levitus et al. 2005). This pattern fits the trend found along the
east coast in which areas farther north experience a greater increase in water
temperature than stations farther south (Maul et al. 2001).
Narragansett Bay is located geographically just below Cape Cod, the
demarcation between northern boreal and southern warmer species (Nixon
et al. 2009). As a result, though it is considered a temperate estuary, it houses
many northern and southern species both on the edges of their zones (Collie
et al. 2008). Many marine organisms already live close to their thermal tolerances
(Somero 2002); as such, even a slight increase in water temperature
could negatively affect their survival (Harley et al. 2006). There have been
many effects of increased water temperature at the organism level in Narragansett
Bay over the past 100 years.
Changes in the winter–spring bloom cycle
In Narragansett Bay, phytoplankton is the major primary producer (Pratt
1959, Smayda 1957). From the 1970s to 1990s, there was a 50% reduction
in annual chlorophyll biomass, a proxy for phytoplankton, in the Bay (Li
and Smayda 1998). This decline has continued through 2006 to an almost
70% decrease in chlorophyll biomass since the early 1970s (Fulweiler and
Nixon 2009). Additionally, phytoplankton phenology has shifted as there has
been a decrease in winter–spring bloom biomass (Oviatt 2004), and in some
instances there has been an absence of the bloom all together (Oviatt et al.
2002). Several factors moderate phytoplankton growth in the Bay, including
bottom-up control by factors such as nutrients and top-down control by
grazers such as zooplankton (Keller et al. 1999).
Over the last 120 years, Narragansett Bay has changed dramatically as
a result of the industrial revolution and the urbanization of Rhode Island
(Hamburg et al. 2008, Nixon et al. 2008). Nutrient input has increased in
the Bay during this time and has also become concentrated in the upper bay
region closer to the city of Providence (Hamburg et al. 2008, Nixon et al.
2008). The exact amount of the increase over the past few decades is unclear,
as different models yield different results depending on input parameters
and assumptions made in the model. Nitrogen input into Narragansett Bay
has been calculated to have increased between 14% (Nixon et al. 2008) and
39% (Hamburg et al. 2008). Water-column production has been found to be
positively related to in situ nutrient concentrations through both mesocosm
experimentation (Oviatt et al. 1986) as well as field surveys (Oviatt 2008).
In terms of top-down control, an increase in grazing pressure could
lead to a decrease in the winter–spring phytoplankton bloom. It has been
hypothesized that grazing pressure from zooplankton has increased during
the winter–spring period due to warmer winter water temperatures (Edwards
and Richardson 2004, Oviatt 2004). The winter–spring phytoplankton bloom
cycle itself is independent of temperature changes (Hitchcock and Smayda
1977, Pratt 1965) and is instead dependent on light levels (Hitchcock and
Smayda 1977) and grazing pressure (Pratt 1965). So as the temperature
changes in the Bay, the winter–spring phytoplankton bloom cycles will not
2010 L.M. Smith, S. Whitehouse, and C.A. Oviatt 81
shift in concert. Thus, whereas diatom phytoplankton once bloomed in advance
of peak zooplankton activity, they now experience increased grazing
pressure early in their spring bloom cycle (Edwards and Richardson 2004),
effectively suppressing the bloom (Oviatt 2004). Patterns of this nature can
be seen in phytoplankton interannual variation from 1977 to 2000 reflecting
cold versus warm years (Oviatt 2004). These findings are reinforced through
mesocosm experimentation in which a 1 °C increase in water temperature
was shown to lead to a reduction in the winter–spring phytoplankton bloom
(Keller et al. 1999). Historically, the winter–spring bloom was a large contributor
to total annual chlorophyll-a production (Oviatt 2004), and thus,
climate change may be a large factor in the observed decrease in annual average
chlorophyll-a levels (Fulweiler and Nixon 2009, Li and Smayda 1998).
The suppression of the winter–spring phytoplankton bloom may be
stressing the benthos (Ellis 2002). In the past, phytoplankton from the winter–
spring bloom that were not grazed sank to the bottom and served as a key
resource for the detritivores that dominate the benthos (Keller et al. 1999,
Oviatt 2004, Rudnick and Oviatt 1986), but with the elimination/weakening
of the spring bloom, less nutritious zooplankton fecal pellets sink to the
benthos instead of nutrient-rich phytoplankton. In the mesocosm experiment
referenced above, warmer water led to a halving of the phytoplankton
biomass that was produced during the spring bloom period and sank to the
benthos (Keller et al. 1999). This change in the downward transport of food
has led to alterations in the benthic community, e.g., decrease in polychaete
marine worms (Ellis 2002).
There are other potential mechanisms that could cause the observed changes
in the phytoplankton spring bloom, e.g., weather oscillations and changes in
fish populations. In 1998, the observed shift in the spring bloom was caused by
the warmer El Niño winter (Oviatt et al. 2002). Another potential mechanism
could be shifts in ctenophore populations (Sullivan et al. 2001), as ctenophores
are voracious predators of zooplankton (Deason and Smayda 1982). Changes
in the composition of fish communities in Narragansett Bay are significantly
correlated with the decrease in chlorophyll-a concentration over the past 50
years (Collie et al. 2008). Specifically, demersal fish abundance is positively
correlated and pelagic fish abundance negatively correlated to chlorophyll-a
concentration (Collie et al. 2008). More research will be needed to sort out the
relative importance of and synergies among these different mechanisms which
may impact the spring phytoplankton bloom.
Changes in fish populations
Historically, overfishing was an important factor in the decline of many
fish populations, yet the increase in bay temperatures is becoming a large
contributing factor in creating conditions unfavorable for many fish species
(Collie et al. 2008, Oviatt et al. 2003). For example, there has been a
decrease in cold-water demersal species and an increase in warm-water pelagic
fish species (Collie et al. 2008, Oviatt et al. 2003). This shift towards
warm-water species is exhibited in mean weighted temperature preference
82 Northeastern Naturalist Vol. 17, No. 1
of fish and invertebrates in the Bay by 2 °C from 1959 to 2005 (Collie et
al. 2008). Specific decreases have been seen in three demersal fish species:
Pseudopleuronectes americanus (Walbaum) (Winter Flounder), Merluccius
bilinearis (Mitchell) (Silver Hake), and Urophycis chuss (Waldbaum) (Red
Hake) (Collie et al. 2008). Increases have been seen in two species of warmwater
pelagic fish (Peprilus triacanthus (Peck) [Butterfish] and Stenotomus
chrysops (L.) [Scup]); four species of invertebrates (Homarus americanus
Milne Edwards [American Lobster], Cancer irroratus Say [Atlantic Rock
Crab], Cancer borealis Stimpson [Jonah Crab], and Loligo pealeii Lesueur
[Longfin Inshore Squid]); as well as one elasmobranch (Leucoraja erinacea
(Mitchell) [Little Skate]) (Collie et al. 2008).
Cold-water fish species are unable to effectively reproduce in warmer
water (Jefferies 1994, Jefferies and Johnson 1974), and so Winter Flounder
numbers have decreased 90% since 1980 in the Bay (Oviatt 2004). Hypotheses
regarding the mechanisms for this decline in the Winter Flounder
population include an increase in larval predation and sub-optimal conditions
for spawning due to increased winter water temperatures over the
past 35 years (Collie et al. 2008, Jefferies 1994, Jefferies and Johnson
1974, Oviatt et al. 2003). Peak spawning of Winter Flounder occurs when
temperatures are between 2 and 5 °C and predators are normally either
absent or inactive (Jefferies 1994, Jefferies and Terceiro 1985, Pereira
et al. 1999). Egg survival, percent hatch, time to hatch, and initial size
of Winter Flounder larvae are correlated with cooler springs (Keller and
Klein-MacPhee 2000). With increasing winter water temperatures, the
predacious shrimp Crangon septemspinosa Say (Grey Sand Shrimp) has
remained active through more of the winter and thus has been able to prey
on Winter Flounder larvae at times when historically the shrimp would be
dormant (Jefferies 1994, 2001; Taylor and Collie 2003; Whitehouse 1994).
If the temperature increases predicted for the Bay in the near future result
in the water never going below 5 °C, Winter Flounder may not lay their
eggs in the Bay or the increasingly active predators may consume all of the
eggs. In addition to low reproductive success, fewer Winter Flounder are
re-entering the Bay, possibly due to offshore exploitation (Jefferies 2001),
further reducing populations in the Bay.
At the same time as a decrease in demersal fish species has been observed,
populations of invertebrates have been increasing. For the two-decade period
starting in the late 1970s, decapods such as Cancer crabs and American
Lobster populations in the Bay have been increasing (Collie et al. 2008, Oviatt
2004). Biomass, as measured from trawl surveys, indicate that the 57%
biomass reduction in fish biomass from the early 1980s to the late 1990s is
roughly equivalent to the increase in decapod biomass during that same time
period (Oviatt 2004). This shift may reflect a decline in predation of decapods
by smaller demersal fish populations (Collie et al. 2008, Oviatt 2004). This
shift has also resulted in increased taxonomic diversity in the Bay as fish have
been replaced by invertebrates of multiple phyla (Collie et al. 2008).
2010 L.M. Smith, S. Whitehouse, and C.A. Oviatt 83
The fish community of Narragansett Bay over the past 47 years is
characterized by an increasing number of fish of a decreasing mean size
(Collie et al. 2008), a pattern consistent with overfishing and climate
change (Collie et al. 2008). These two forces acting in concert have the
potential to reduce fish population sizes to levels below which they can not
recover (Scavia et al. 2002). Other factors, such as decreased chlorophyll-a
concentration, a shift towards positive Atlantic Multidecal Oscillation
(AMO) cycles (Collie et al. 2008), and eutrophication (Deacutis 2008),
also play a role in fish species composition shifts in the Bay. These factors
will also interact with fishing effort and stock size (Harley et al. 2006).
Change in precipitation
Though global-scale changes in precipitation are highly variable, a
significant trend of increasing precipitation can be seen in eastern North
America (IPCC 2007). In the New England region, precipitation has increased
4% (3.8 cm) from 1895 to 1999 (New England Regional Assessment
Group 2001). Just as with the temperature, Rhode Island has seen a larger
increase in precipitation—27% (30 cm)—during the same time period (New
England Regional Assessment Group 2001, Pilson 2008).
In addition to increasing total precipitation, there has been an 88%
increase in the frequency of extreme precipitation events in Rhode Island
since 1948, the largest increase of any state in the United States (Madsen
and Figdor 2007). Extreme precipitation events are defined as all events with
the 24-hour precipitation total greater than the smallest of the maximum
annual precipitation events for each year of the 59-year study (Madsen and
Figdor 2007). The limited available data means that the confidence interval
associated with this increase is quite large (24% to 152%). The 10% increase
in freshwater input to the Bay since 1960 (Pilson 2008) is likely the result
of the changing precipitation patterns and could have far reaching consequences
for the Bay, e.g., decreasing salinity, and increasing stratification,
turbidity, and terrestrial-derived nutrient inputs (Harley et al. 2006). The
impacts caused by increased precipitation will be compounded by hydrograph
changes caused by urban development and wetland losses (Rogers and
Tropical cyclone intensity has increased in the North Atlantic over the
past 40 years (Goldenberg et al. 2001, Meehl et al. 2007, Solomon et al. 2007,
Trenberth et al. 2007, Webster et al. 2005) as illustrated by the doubling of
the number of category 4 and 5 tropical cyclones since the 1970s (Webster
et al. 2005). The strength of tropical cyclones is predicted to continue to
increase in the North Atlantic over the next century (Emmanuel 2005, Mann
and Emanuel 2006, Scavia et al. 2002). Though globally the number of tropical
cyclones is predicted to remain the same or even decrease, the number
of hurricanes in the North Atlantic has been and will continue to increase
(Oouchi et al. 2006, Webster et al. 2005). Increased tropical cyclone intensity
could have large effects on Rhode Island beaches, with greater storm
surges overwashing more barrier beaches, redistributing their sediment, and
84 Northeastern Naturalist Vol. 17, No. 1
more frequently breaching the barrier beaches (Morton and Sallenger 2003).
This increase in barrier breaches could have large effects on coastal lagoonal
ecosystems in southern Rhode Island, increasing the flushing rate and salinity
of the lagoons (Bird 1994, Smith 1994).
Damage from a major hurricane if it were to strike in the future would
be particularly devastating for Rhode Island given its increasingly coastal
demographics; there has been an approximate doubling in population
and wealth of the population in coastal counties from 1938 to 1995 (Pielke
and Landsea 1998). The last category-3 hurricane to directly impact the Bay,
the hurricane of 1938, caused $3.6 billion (1995 dollars) in damage in New
York, Connecticut, Rhode Island, and Massachusetts combined (Pielke and
Landsea 1998). If that same hurricane were to have hit the region in 1995,
the damage would have been approximately $16.6 billion (1995 dollars;
Pielke and Landsea 1998).
Sea level has increased by 13 cm from 1931 to 2007 in Narragansett Bay,
as recorded in long-term data from NOAA tide gauge stations in Providence
(#845400) and Newport (#8452660) (Fig. 3). With so much of the population
living along the coast, this sea-level rise will have potentially large
negative economic and ecologic impacts. The observed rate of increase of
0.17 m/century is the same as the observed average global rate (IPCC 2007).
Increasing global rates of warming will accelerate rates of sea-level rise
globally and locally (Meehl et al. 2007, Overpeck et al. 2006).
In the Narragansett Bay region, isostatic shifting has lead to land subsidence
of 0.15 m/century (Boothroyd et al. 1998), thus the total elevational
shift along the coast of Rhode Island over the past century is about
Figure 3. Annual average sea level in Narragansett Bay as derived from NOAA tide
gauges in Newport (#8452660) and Providence (#845400), RI. The data represent the
difference from mean sea level. Mean sea level is defined and determined by NOAA as
the arithmetic mean of hourly tidal heights observed from 1983–2001. Thus, a negative
number would indicate that the annual mean was lower than mean sea level for
that location, and a positive number would indicate the annual mean was higher than
mean sea level. Data was accessed at: http://tidesandcurrents.noaa.gov.
2010 L.M. Smith, S. Whitehouse, and C.A. Oviatt 85
0.29 m/century. This combined shift means that upland lands near lowland
tidal areas are being flooded, beach erosion has increased, and barrier islands
are migrating at increasing rates (Scavia et al. 2002). Additionally, rising
water tables resulting from these factors will cause increased failures in septic
and storm drainage systems in more than half of the state’s coastal areas
(Bertness and Ewanchuk 2002, Sea Grant 2004). If the combined rate of sealevel
rise and land subsidence exceeds the accretion rate of the salt marsh,
salt marshes will be inundated, leading to the destruction of large areas of
these critical ecosystems (Donnelly and Bertness 2001). Presently, the accretion
rate of low- and high-marsh habitats, 0.43 cm per year and 0.24 cm per
year, respectively (Bricker-Urso et al. 1989), still exceeds the combined rate
of subsidence and sea-level rise in Rhode Island, yet that is not predicted to
be the case in the future (Meehl et al. 2007).
The sediments of Rhode Island’s barriers and headlands are glacially derived
and as such are highly susceptible to increased erosion resulting from
sea-level rise, with the south shore of Rhode Island being particularly vulnerable
(Boothroyd 1999). Currently, the south shore is retreating on average
30–70 cm per year (Sea Grant 2004), reflecting the joint effects of sea-level
rise (long-term factor) and sporadic extreme events (short-term factors). Increases
in sea level have an additive effect when coupled with storm surge,
causing waves to break higher on bluffs and dunes during coastal storms
(Boothroyd et al. 1998). Even an increased storm surge of 25–50 cm can
greatly increase erosion rates (Boothroyd 1999).
Several factors influence the variability of pH in seawater, such as
changes in the concentration of total dissolved CO2, alkalinity, and temperature
(Hinga 2002). The magnitudes of these variations in pH are linked
to the salinity of the seawater, as the concentration of salt influences the
pH-buffering properties of the seawater (Hinga 2002). As a result, the pH
of Narragansett Bay is more variable than the pH of the open ocean, showing
a fluctuation of >0.5 units above or below the equilibrium depending on
seasonal productivity cycles (Hinga 2002) and variation in freshwater input
(Mitchell and Rakestraw 1933, Mitchell and Solinger 1934). As a result, the
effects of an overall decrease in pH resulting from increased atmospheric
concentrations of carbon dioxide may be different in Narragansett Bay than
in the open ocean. Compounding the influence of increasing carbon dioxide
are the effects of chronic eutrophication of Narragansett Bay (Hinga 2002).
Further research is needed to untangle the net effects of decreasing in pH in
Narragansett Bay and coastal Rhode Island have been negatively affected
by climate change, and these effects are likely to worsen as warming and CO2
concentrations increase. With the long residence time of CO2 in the atmosphere
86 Northeastern Naturalist Vol. 17, No. 1
(100 years on average) and the even longer residence time in the ocean (1000 to
1500 years), any emissions reductions we make now will not positively influence
the environment for many years. It is essential not only to look at global
averages of climate change but also at changes in specific regions, as they will
differ greatly. For instance, ecosystem change in Narragansett Bay can impact
fish populations, which in turn can have significant effects on commercial and
recreational fishermen. Increased erosion along the coastline can damage property
and lead to the loss of valuable beaches. Additionally, there are increased
threats of flooding and property damage by hurricanes.
We thank Senator Sheldon Whitehouse for so graciously hosting this literature
review. The research was sponsored by NSF IGERT grant #0504103 to the University
of Rhode Island Coastal Institute. We also wish to thank Rele Abiade, Mindy Meyers,
and George Carvalho from Senator Whitehouse’s office for their mentorship on
this project. We also thank Dr. Michael Pilson, Dr. John Merrill, Dr. Steven Hamburg,
Don Pryor, Gail Scowcroft, Russell Perry, Dana Smith, Russell Smith, Warren
Schudy, the Coastal Institute IGERT Project (CIIP) faculty, and CIIP trainees for
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