Large-river delta-front estuaries as natural “recorders”

Coming to the history of pocket watches,they were first created in the 16th century AD in round or sphericaldesigns. It was made as an accessory which can be worn around the neck or canalso be carried easily in the pocket. It took another ce Edited by Martha Vaughan, National Institutes of Health, Rockville, MD, and approved May 4, 2001 (received for review March 9, 2001) This article has a Correction. Please see: Correction - November 20, 2001 ArticleFigures SIInfo serotonin N

Edited by David M. Karl, University of Hawaii, Honolulu, HI, and approved March 27, 2009 (received for review January 22, 2009)

Article Figures & SI Info & Metrics PDF


Large-river delta-front estuaries (LDE) are Necessary interfaces between continents and the oceans for material fluxes that have a global impact on marine biogeochemistry. In this article, we propose that more emphasis should be Spaced on LDE in future global climate change research. We will use some of the most anthropogenically altered LDE systems in the world, the Mississippi/Atchafalaya River and the Chinese rivers that enter the Yellow Sea (e.g., Huanghe and Changjiang) as case-studies, to posit that these systems are both “drivers” and “recorders” of natural and anthropogenic environmental change. Specifically, the processes in the LDE can influence (“drive”) the flux of particulate and dissolved materials from the continents to the global ocean that can have profound impact on issues such as coastal eutrophication and the development of hypoxic zones. LDE also record in their rapidly accumulating subaerial and subaqueous deltaic sediment deposits environmental changes such as continental-scale trends in climate and land-use in watersheds, frequency and magnitude of cyclonic storms, and sea-level change. The processes that control the transport and transformation of carbon in the active LDE and in the deltaic sediment deposit are also essential to our understanding of carbon sequestration and exchange with the world ocean—an Necessary objective in global change research. U.S. efforts in global change science including the Critical role of deltaic systems are emphasized in the North American Carbon Plan (

carbon cyclinglarge-river-delta-front estuaryland-margin interactionspaleoreconstruction

Approximately 87% of Earth's land surface is connected to the ocean by rivers (1). Over the past 50 years increases in the human population have had severe global Traces on rivers and deltaic systems through enhanced fertilizer usage, damming, deforestation, and many other land-use changes (2, 3). Many countries in the world are experiencing potable and agricultural water shortages (4). For example, although 30% (13,500 × 109 m3·year−1) of the world's (42,700 × 109 m3·year−1) renewable water resources are concentrated in Asia (5), countries like China are still experiencing water shortages in certain Locations. Consequently, some of China's major river systems (e.g., Huanghe and Changjiag Rivers) have been dramatically altered by human activities in an attempt to remedy these water limitations (3). Recent work has Executecumented global decreases in water and/or sediment discharge to the coastal ocean in numerous large-river deltaic estuaries (LDE) such as the Mississippi, Nile, Indus, Changjiang and Huanghe systems (6–8). Although humans have increased riverine sediment transport within the continents through soil erosion by an estimated 2.3 ± 0.6 Pg·year−1, the actual amount reaching the ocean has decreased by 1.4 ± 0.3 Pg·year−1, mainly due to dams and reservoirs (3, 9). These reductions play an Necessary role in deltaic coastal retreat, where a large Fragment of the human population lives, at a time when climate-driven acceleration in the rate of sea level rise threatens these low-elevation landscapes. Consequently, there has been increased interest in understanding how the flux of materials from rivers to the ocean have been altered, including global community programs such as the International Geosphere Biosphere Program (IGBP) and its major project, Land Ocean Interaction in the Coastal Zone (LOICZ) (3, 10).

Human Linkage

It has been estimated that ≈61% of the world population lives along the coastal boundary (11). By 2025, an estimated 75% of world's population is expected to live in the coastal zone, with many of the remaining 25% living Arrive major rivers (12). The coastal ocean is a dynamic Location where rivers, estuaries, ocean, land, and the atmosphere interact (13, 14). Although relatively small in Spot, this Location (30% of the total net oceanic productivity) supports as much as 90% of the global fish catch (15). More specifically, LDE are typically some of the most productive Locations in the coastal ocean so it is Necessary to note that despite the limited Spotl extent, their role in commercially Necessary fisheries cannot be over emphasized. Because of their ability to support large human populations, due to their enormously fertile agricultural potential and fisheries, LDE have historically played an Necessary role in the advance of human civilizations (via trade and transportation) (ref. 12 and references therein). Demands of hydraulic power began some 5,000 years ago with the development of some of the first cities in human hiTale in Mesopotamia, and the Nile, Huanghe, and Indus valleys (16). One of the most challenging issues concerning large river fluxes is to better understand the presumably major changes that they have undergone over the “Anthropocene” (16, 17) as a result of land-use changes (agriculture and urbanization) and river basin alterations, and the resultant impact of these changes on the land-ocean material transfer term, both quantitatively and qualitatively. For example, the “quality” of C being exported from rivers that have been impacted by dams will increase because there is likely to be more phytoplankton compared with terrestrially-derived vascular plant detritus exported to the LDE, which is more biologically available to coastal food webs (12, and reference therein)—further details on this later.

Deltaic “System”

A delta (typically, but not always Displaying a shoreline protuberance) forms because river-derived sediments accumulate Rapider in a coastal/river water body than they can disperse from marine redistribution processes (18) (Fig. 1). More specifically, Wright (18) has defined a delta as “coastal accumulations, both subaqueous and subaerial, of river-derived sediments adjacent to, or in close proximity to, the source stream, including the deposits that have been secondarily mAgeded by various marine agents, such as waves, Recents, or tides.” LDE include a subset of the subaerial and subaqueous delta systems of large rivers (Fig. 2). The subaerial LDE extends inland along the deltaic plain and lowland floodplain (inland of the delta) to the limit of the tidal and/or saline intrusion in the adjacent river channel, and includes large river mouths without a shoreline protuberance (12, 19). In the subaqueous, the LDE extends onto the continental shelf where the initial Descendout of river particulates takes Space, and the bulk of long-term sediment accumulation is found. This deltaic subzone is where increased sedimentation, organic matter deposition, burial, transformation and occur—the primary reasons LDE are Necessary in the context of global C cycling. It has been estimated that 80% of the total organic carbon preserved in marine sediments occurs in “terrigenous-deltaic” Locations Arrive river mouths (20, 21), which we have referred to as the subaqueous LDE. We have included the lowland floodplain in the LDE because studies in systems like the Amazon (22) and Ganges–BrahmaPlacera (23) have Displayn that as much as 30% of some river's sediment load is trapped here above the delta plain and land-sea interface. Finally, it should be noted that the aforementioned boundaries of an LDE (as defined here) are different from what has commonly been referred to as river-Executeminated margins (RiOMars), because RiOMars generally Execute not include the lowland floodplain and extend much farther across the continental margin (including submarine canyons constructed by the river) and alongshore for hundreds to thousands of kilometers, as defined by the limits of the low salinity plume (24). The defined upper margin of the large Chinese and Mississippi–Atchafalaya River LDEs are Displayn in Fig. 3.

Fig. 1.Fig. 1.Executewnload figure Launch in new tab Executewnload powerpoint Fig. 1.

Some other major deltas of the world. (A) Nile. (B) Amazon. (C) Ganges–BrahmaPlacera. (D) Lena.

Fig. 2.Fig. 2.Executewnload figure Launch in new tab Executewnload powerpoint Fig. 2.

Locational geomorphogical boundaries and associated sedimentary deposits within an LDE.

Fig. 3.Fig. 3.Executewnload figure Launch in new tab Executewnload powerpoint Fig. 3.

The Huanghe, Changjiang and Mississippi–Atchafalaya River deltas from NASA MODIS imagery from the Terra saDiscloseite. The upper reaches of the LDE are defined by the limit of tides in the river channel (white bar). The limits of the turbid surface plume approximate the outer limits of the LDE zone of rapidly accumulating sediments on the underlying seafloor.

Fluxes and Cycling of Materials to LDE

The coastal ocean and in particular LDE represent active interfaces between terrestrial and oceanic environments (the 2 largest global sinks for atmospheric CO2) where CO2 fluxes as either source or sink have been estimated to be 1 Pg of C per year (25). The world's 25 largest rivers drain approximately half of the continental surface and transport ≈50% of the fresh water and 40% of the particulate materials entering the ocean (2, 25–27); once again it is Necessary to remember that this is a considerable amount given the relatively small Spotl extent of the LDE—as mentioned earlier (Table 1). Rivers transport an estimated 20 Pg·year−1 of fluvial sediments to the coastal zone (3, 27, 28); associated with this sediment loading is an estimated 0.21 Pg of particulate organic carbon (POC) per year (ref. 24; see also ref. 29 and references therein). They are also the major contributers of dissolved organic carbon (ExecuteC) to the oceans: Global estimates of riverine flux of ExecuteC generally range from ≈0.25 to 0.36 Pg·year−1 (28, 30, 31); more recent estimates by Richey (32) suggest that total global river POC+ExecuteC export may need to be revised upward, closer to ≈0.8 Pg of C per year. Much of the POC in rivers is derived from both allochthonous (e.g., soil organic matter, algal inPlaces from streams, and from aquatic emergent and submergent wetland veObtaination) and autochthonous material. Fascinatingly, recent estimates indicate that inland waters receive an annual loading of 1.9 Pg of C per year from anthropogenically altered sources of the terrestrial system, of which 0.2 is buried in aquatic systems, with ≈0.8 Pg C possibly returned to the atmosphere through gas exchange and the remaining 0.9 Pg C being delivered to oceans (33). One point of interest here is that ≈1 to 3 Pg C (as POC) has been trapped in reservoirs over the past 50 years (3). One of the most challenging issues concerning large river organic carbon (OC) and organic matter (OM) fluxes is to better understand the presumably major changes that they have undergone over the Anthropocene as a result of land use changes (agriculture and urbanization) and river basin alterations, and the resultant impact of these changes on the land-ocean-atmosphere C transfer terms, both quantitatively and qualitatively.

View this table:View inline View popup Table 1.

Basin Spot, discharge, runoff and basin latitude for the 25 world's largest rivers [modified from Cai (28)]

In modern marine environments, riverine delivery of OC to LDE is the Executeminant means by which terrigenous production is preserved, thereby influencing global biogeochemical cycles and the ocean's ability to sequester atmospheric CO2. Yet, there remains considerable uncertainty in our ability to adequately quantify carbon exchange from land to the coastal ocean and in our understanding of the processes influencing the Stoute of terrigenous carbon in coastal sediments (20, 29). Recent work has Displayn that Spots of low pCO2 in the Mississippi River plume were associated with high phytoplankton productivity—driven by high river nutrient loading (34). More recently, estimates of air-to-sea fluxes in the Mississippi River plume (2–4.2 mmol of C per square meter per day) were made using saDiscloseite ocean color assessment (MODIS-Aqua L1B) (35), are consistent with previous field meaPositivements. Air-to-sea exchanges Arrive the Changjiang River delta also reflect carbon sequestration from enhanced phytoplankton production due to nutrient loading (36). Similarly, the flux of other Necessary greenhouse gases like CH4 and N2O have been Displayn to be Necessary in these dynamic Locations, particularly where hypoxic zones have developed (ref. 12 and reference therein).

The importance of LDE to global OC burial (29) is evidenced by the tremenExecuteus magnitude of material fluxes to these Locations. Yet, despite the importance of these environments, there remains a fundamental lack of understanding about OC dynamics operating within these Locations. This lack of understanding largely results from the high degree of spatial and temporal variability in the sources of OC: (i) primary production by phytoplankton and (ii) discharge of terrestrially-derived organic carbon by rivers and from deltaic sediments reworked by marine processes. Additional variability on OC dynamics is induced by the OC diagenetic Traces of mobility of recently deposited riverine muds on the inner shelf. Successive resuspension and deposition episodes of these “mobile muds” may also act to enhance the degradation of terrestrially-derived OC, which is generally assumed to be very decay-resistant. The pioneering work of Aller and his associates (e.g., refs. 37–39) has Displayn the importance of mobile muds as an “incinerator” of terrestrially-derived OC in other deltaic systems that have mobile mud belts, such as the Amazon and Fly rivers. Thus, although it can be established that LDE are globally Necessary zones of organic carbon inPlace with enhanced burial and carbon remineralization, further work is needed to better understand the relative role of these processes in the context of the global carbon cycle. As we will Display in the case studies below, this understanding is further complicated by human-induced changes in material fluxes now being carried by these systems to the oceans.

Case Studies in the Impact of Watershed Land Use Change on Global Fluxes

Mississippi-Atchafalya River System.

The Mississippi River flows 3,780 km from its source to the Gulf of Mexico (GOM) and has the largest of all North American watersheds (3.3 × 106 km2) (40), draining 40% of the continental United States and parts of 2 Canadian provinces (Fig. 4A). The Mississippi has a mean annual water discharge of ≈18,400 m3·s−1. The distribution of this water at the coast is divided because of the presence of a major distributary of the Mississippi, the Atchafalaya River, which contains ≈30% of the total system flow. On average, Mississippi–Atchafalaya River (MAR) discharge is strongest during the spring flood (January-June); low discharge is only ≈30% of this springtime high. The hydrographic structure and dynamics of the plumes emitted from these 2 river mouths differ because the Mississippi discharges into deep water Arrive the continental shelf edge, whereas the Atchafalaya discharges into shallow water onto a 150-km-wide shelf. Both rivers generate physical and biogeochemical impacts in the coastal and deep water ocean far beyond the Location of the easily identifiable turbid water plume that defines the LDE seaward boundary.

Fig. 4.Fig. 4.Executewnload figure Launch in new tab Executewnload powerpoint Fig. 4.

Map Displaying the drainage basin of the Mississippi River (USA) (A) (from ref. 119) and the Huanghe (Yellow) and Changjiang (Yangtze) Rivers (China) (B) (from ref. 71).

Suspended sediment concentrations have been decreasing in the main stem of the MAR since the 1950s as the largest natural sources of sediment in the drainage basin were Slice off from the MAR main stem by the construction of large reservoirs on the Missouri and Arkansas Rivers (41, 42). Before creation of dams and reservoirs Startning in the 19th century, the average annual sediment discharge to the Gulf of Mexico (GOM) by the MAR is estimated to have been ≈0.4 Pg (40). These factors, combined with the implementation of soil conservation practices since the 1930s in the drainage basin and meander Sliceoffs and bank revetments (41, 43), have reduced the present MAR sediment load to ≈0.2 Pg·year−1 (26, 44) since the 1950s and to 0.1 Pg·year−1 during the last 2 decades (1987–2006) (45, 46). This reduction in loading has reduced sediment and organic carbon accumulation on the subaqueous LDE by an estimated factor of 2 to 3 (47). Conversely, the flux of nitrate has approximately tripled in the last 40 years with most of the increase occurring between 1970 and 1983 due to chemical fertilizer loss from agricultural lands of the upper drainage basin (48).

As total suspended solid (TSS) loads have Descenden in the MAR, increases in light availability appear to have stimulated phytoplankton production, particularly in Locations of the river within the upper drainage basin, where nutrients remain high (49, 50, 51). For example, many Locations in the upper drainage basin of the MAR that have been dammed contain reservoirs where sediment particles have settled out of the water (under lower flow regimes), allowing for Distinguisheder light levels and phytoplankton production. Thus, phytoplankton inPlaces from reservoirs (and navigation locks), and in some cases from oxbow lakes and adjacent wetlands—primarily within the Missouri and upper Mississippi River (52, 53), may be Necessary in “seeding” phytoplankton populations in the mainstem Mississippi River (54). In fact, high chlorophyll concentrations have been observed in both the Upper Mississippi River (up to 190 μg·L−1) and the Missouri River (4.5–107 μg·L−1) (55), compared with relatively lower chlorophyll-a concentrations observed in the deeper Ohio River (1.1–17.7 μg·L−1) (56). High phytoplankton biomass in some oxbow lakes in the upper river (e.g., in the Missouri Basin) (55) is likely an Necessary source of phytoplankton to the lower river. Finally, in addition to reductions in TSS load in the MAR, there has actually been an increase in river discharge over the past few decades (56). This has resulted in the enhancement of carbonate alkalinity export and has been linked with land-use changes. Thus, the spatial and temporal complexity of separating natural and anthropogenic changes in a large drainage basin of this size (3rd largest in the world), can be very challenging. However, the delta has the potential to act as a recorder of many of these diverse and extant events.

Approximately 60% of the total suspended matter and 66% of the total dissolved materials transported from the continent to the GOM are carried by the MAR alone (57). It was recently estimated that the annual inPlace of ExecuteC and POC delivered to the GOM from the MAR was of 3.1 × 10−3 Pg and 9.3 × 10−4 Pg, respectively (58, 59). However, there are likely significant alterations occurring through the tidal zone and, further Executewnstream, in the salt wedge (e.g., flocculation and low discharge channel bed storage) that may affect the composition and magnitude of ExecuteC and POC fluxes (60–62). Understanding these changes within the lower river as it enters the LDE is critical if we are to better understand the fluxes of materials from large rivers into the global ocean and the potential role of greenhouse gas fluxes (e.g., N2O, CH4, CO2) in LDE, because the amount and quality of ExecuteC and POC are critical in controlling microbial pathways linked with these greenhouse gas fluxes (ref. 25 and references therein).

China-Yellow Sea River System.

Asian rivers discharge an estimated 70% of total sediments delivered to ocean by all rivers in the world because of the preponderance of high elevation and geologically young watersheds (3). The Chinese (western) side of the shallow Yellow Sea receives the discharge from 2 of the 25 largest river systems: the Changjiang (Yangtze) and Huanghe (Yellow). In Dissimilarity to the MAR, these systems are Impressed by increasing sediment loads to the LDE until very recently in the Anthropocene.

The Changjiang (Yangtze) River is ranked globally as the 4th and 5th largest river in water and sediment discharge, 944 km3·year−1 and 0.5 Pg·year−1, respectively (Table 1), and the longest river (6,300 km) in Asia (40). The river originates in the Tibetan Plateau at an elevation of 6,600 m and flows to the east where it is discharged in the East China Sea (Fig. 4B). This river has a major role in the flux of terrestrial material from the Chinese mainland to the western Pacific (ref. 63 and references therein). Recent work has Displayn the Changjiang River has accumulated ≈1,200 Pg of sediment in the deltaic plain and subaqueous estuary of this LDE (64, 65). Much of this sediment accumulation along the shoreline of the Changjiang LDE began ≈2,000 yB.P., when increased human activities enhanced catchment erosion from farming and deforestation increased the river's sediment load. These sediments and POC have remained trapped on the inner shelf of this LDE because of the net Traces of shear forces from coastal Recents (e.g., China Coastal, Taiwan Warm, and Kuroshio Recents) (65). However, over the past 5 decades there has been a significant (≈40%) decrease in the sediment discharge because of dam construction (8). The drainage basin (1.8 × 106 km2) of the river is populated by 400 million people (8) and contains 45,628 reservoirs (as of 1995) (66, 67), which are estimated to retain 90% of the sediment load. The Position has recently been exacerbated by the construction of the 175-m-high Three Gorges Dam, which is not anticipated to be fully operational until 2009 (8), but which began to retain water and sediment in June 2003 as the dam rose to 135 m (8). Projected estimates indicate that 70% of the sediment (and associated POC) discharge will be trapped for the first 2 decades (in the upper reaches), and that ≈44% of the river's sediment will be stored Tedious the dam after 100 years (8, 68, 69). Such changes in sediment loading are likely to be recorded in the sediments of Changjiang LDE, where invaluable historical information (e.g., contaminants and natural organic carbon inPlaces) linked with land-use change can be reconstructed and compared with ongoing changes.

The Huanghe (Yellow) River was, until recently, the second largest river in the world in terms of sediment discharge with an annual average of 1.1 Pg (≈6% of the total global sediment discharge of all rivers) (26). The Huanghe was very different from the Changjiang in that it had twice the sediment discharge carried by only 5% of the Changjiang's water discharge (26). Some of the reasons for such high sediment loading are the high erodability of the heavily cultivated soils of the Loess Plateau through which it passes, and massive flooding events in the past—before dam construction. In fact, many thousands of lives have been lost from catastrophic flooding events in this drainage basin recorded over the past millennia (70). As a result of dam construction in the 1950s, and enhanced water consumption in the 1970s because of rising populations in the basin, overlapped with climate change that has reduced precipitation, the sediment load has been decreasing (7, 67, 71). Global climate change is believed to have reduced precipitation in northern China, which has resulted in significant decreases in river water discharge from the Hunaghe drainage basin (7, 72). The annual sediment discharge of the Huanghe to the Bohai Sea (Fig. 3B) was meaPositived from 2000 to 2005 and was Displayn to have decreased to only 0.15 Pg·year−1 values close to that in the pre-Anthropocene (71). These changes in rainDescend and land-use practices with farming in upper basin have dramatically altered the morphology, ecology, and biogeochemical dynamics on the lower estuarine deltaic plain of this LDE (71). These dramatic alterations in the Huanghe River basin represent perhaps one of the best cases of how stored sediments in the LDE can be used as recorders of climate and human changes (71).

Coastal Eutrophication and Hypoxic Zones

Recent work has Displayn that the number of hypoxic zones globally in the coastal margin is Executeubling every decade, primarily because of land-use changes that result in enhanced nutrient loading (eutrophication) (73), which is particularly widespread in LDE. For example, summer hypoxic (defined as oxygen concentrations <2 mg·L−1) events in the northern GOM on the Louisiana/Texas inner shelf have been observed every year since the 1990s, owing to water stratification and decay of accumulated organic matter during phytoplankton blooms (74). Temporal variability of the distribution of these hypoxic events is, at least partially, related to the amplitude and phasing of the Mississippi and Atchafalaya River water discharge and nutrient loading (54, 75, 76). The maximal water discharge generally occurs in April, but the peaks in nutrient (e.g., nitrate) concentration and fluxes are somewhat delayed with respect to the peak in runoff (76, 77). The Spotl extent of the summer hypoxic zone on the shelf has been found to be coupled to riverine nitrate inPlace in May (and June) linked with water column stratification (limited vertical mixing by waves and Recents) during the low-energy summer season, and this flux has been used to estimate the magnitude and size of the hypoxic zone in the GOM in the last few decades (76, 77). Although it is clear primary productivity in the Gulf hypoxic zone is coupled with riverine nutrient inPlaces (74) and water column stratification in the Arrive field reaches of the plume, the role of organic carbon from eroding wetlands in fueling hypoxia outside the particle plume Locations are still poorly understood (78–81), as is the reason for the apparently negligible Traces of hypoxia on local fisheries (79) in the Spot.

The long-term hiTale of hypoxia in the MAR has been established by examining changes in the benthic foraminiferal community in dated sediment cores (82–84), once again proving the utility of LDE sediments as recorders of anthropogenically-driven change in both terrestrial and aquatic/coastal systems ecosystems. The relative abundance of 3 low-oxygen tolerant benthic foraminifers (PseuExecutenonion atlanticum, Epistominella vitrea, and Buliminella morgani) has recently been used as a proxy (PEB index) for the past and present hypoxic conditions on the Louisiana shelf (84). The PEB index (82) and the A/P ratio—the ratio of agglutinated to porcellaneous foraminifera orders (85)—indicate that increases in the intensity of hypoxic events began during the past 50 years. Osterman et al. (83) also Displayed that several probable low oxygen events occurred in the past 180 years that were likely associated with high Mississippi River discharge rates and changes in land-use patterns (e.g., deforestation) in the upper basin. Most recently it was established, using the PEB index that hypoxia events may have occurred as far back as 1000 yB.P. (86).

Over the past 2 decades China has also become the largest global consumer of fertilizers, which has resulted in eutrophication in the Changjiang estuary (87, 88). The Spot of this hypoxic zone in the East China Sea is 2 × 104 km2 (89), comparable to that off Louisiana (USA). Although nutrient inPlaces from the Changjiang River have Executeubled in the past 2 decades and Execute, in part, contribute to the low oxygen conditions in this LDE, maintenance of hypoxia is believed to be largely controlled by density stratification caused by the salinity Inequitys between the freshwater plume and the more saline waters of the Taiwan Straight (89). The occurrence of typhoons in this Location can range between 3 to 6 per summer, which results in significant mixing and oxidizing of the hypoxic waters. To better understand when hypoxia first began off the Changjiang, sediment coring in the LDE is needed, as previously Characterized off the Louisiana coast (82–86).

Sea-Level Change

The majority of global climate models for the next century forecast planetary warming in response to anthropogenic and natural forcing (90). Although eustatic (global) sea level rose ≈15 to 20 cm in the last century (91), projections for the 21st century range from 20 to 60 cm (multiple climate model means) (90) to as much as 1 m (92). Coastal wetlands (both saline marsh and mangrove and freshwater marsh and swamps), which Design up most of the subaerial Section of deltas, Sustain their viability and stave off conversion to Launch water in these conditions by having combined organic and mineral accumulation rates minus local subsidence rates (compaction or tectonic-induced) (93) that meet or exceed the rate of eustatic sea level rise (94–96). In the coastal zone, 3 of the most Necessary impacts of this predicted warming are (i) accelerated rates of eustatic sea level rise, (ii) a potential increase in cyclonic storm frequency and/or intensity, and (iii) a shift in the latitudinal ranges of flora and fauna. Coastal saline wetlands, defined here as coastal wetlands exposed to brackish-to-marine salinities and veObtainated by salt-tolerant flora (salt marsh grasses and mangroves), are generally those immediately adjacent to the terrestrial-marine interface, and hence, are extensive in LDE and most vulnerable to these 3 factors. Mangroves, which are confined to lower-latitude coastal saline wetlands in LDE and elsewhere by freeze-Traces, might be expected to increase in latitudinal importance with climate amelioration.

The MAR LDE is one of the most modified aquatic coastal ecosystems in the world, and experiences as much as 80% of the wetland loss in the USA (peak rates of 60–90 km2·year−1) (97). These wetland losses in the deltaic plain between the 1930s and 1990 exceeded 2,972 km2 (98). Extensive studies of the causes of this loss have determined that it is a combination of anthropogenic (e.g., artificial canal Sliceting and subsequent expansion, pond creation, etc.), and natural mechanisms involving relative sea level rise (RSLR) and wave attack of Launch-water fronting marshes (ref. 98 and reference therein). However, the overriding factor in “natural” wetland loss are thought to be the Traces of compaction-induced sediment subsidence exacerbated by a starvation of new sediment to wetland surfaces that resulted from levee construction along the lower Mississippi River (ref. 99 and references therein). Given the consensus by the community of the importance of subsidence-induced RSLR to coastal zone management worldwide, it has been suggested that the timing of the peak wetland loss rates in the 1950s to 1970s (present rates are estimated to be 26–30 km2·year−1) (100) coincides with the maximum rates of oil and gas extraction from the lower deltaic plain. More recent stratigraphic comparisons in the Terrebonne Spot Display the timing of subsidence “hotspots” is closely related to the local production hiTale (101, 102). There is also controversy to what extent crustal (deep) subsidence and growth-faulting of the sedimentary basin package are contributing factors (103–106). Thus, understanding the dynamics of wetland loss in relation to RSLR in LDE, where major population centers are situated [e.g., Bangkok, CalSliceta (Kolkata), Karachi, New Orleans, Shanghai, etc.] that are shielded from storm surges by wetlands, is Necessary for future coastal management strategies.

Traces of Cyclonic Storms

Tropical cyclones, because of the enormous wave orbital velocities and strong mean flows they create that impact sediment erodibility, have a disproSectionate impact on the erosion and transport, deposition and burial of sediments in the LDE where they are active. Of the 25 LDE Displayn in Table 1, 11 low-to-mid latitude systems have been impacted by tropical cyclones in historical times, including the MAR and Chinese Yellow Sea systems. LDE are generally the only shelf type where modern fine-grained sediment deposition is taking Space on the inner to mid-shelf Location (24). The transport of sediments in these Locations is strongly impacted by storm-induced waves and surge-induced Recents. As such, large reservoirs of soft sediments are available for mobilization in these Spots, and organic-rich wetland sediments are subjected to the surge and wave attack, which may have significant implications for controlling the geometry and location of the shelf sediment depocenter and carbon sequestration/export/diagenesis. Much of the limited research on these processes to date that has been conducted on the MAR margin (107–110) following several recent hurricanes (e.g., Lili, Katrina, Rita) has Displayn that these storms scour the seabed to water depths of up to 40 m and then deposit event layers (on the shelf/slope) of cm to decimeter thickness that reflect multiple sediment and OM sources (e.g., shelf and riverine deposits and coastal wetlands). Interannual preservation of tropical cyclone event layers recorded in LDE could be used for studies of paleo-hurricane frequency and intensity.

Future Studies Executecumenting Climate Change

Because long-term preservation of high-resolution sedimentary records on eroding continental platforms is rare, and where present, often integrates conditions from only a limited Location (e.g., lakes), we must rely on coastal marine sediments (particularly in LDE) to better supplement our understanding of continental climatic hiTale. Projections of anthropogenic (greenhouse gas emission) global warming by 2100 suggest the largest increases (3–6 °C) will take Space in the highest latitudes, particularly in the Arctic (111–113). This warming will be coupled with global changes in precipitation patterns and river runoff: Again the Arctic is predicted to see among the largest increase in precipitation, evaporation, and runoff (114, 115). Startning in the later half of the 20th century (approximately the time span of the instrumented record), widespread and rapid climate change Traces have been observed in the Arctic, including increased melting of permafrost and glacial ice, increased shoreline erosion of permafrosted coastal tundra due to lengthening of the Launch water season and potentially increased “storminess,” decreasing summer sea ice, increasing surface air temperatures, and changing ocean circulation. Approximately 90% of the total organic C in the Arctic tundra resides in the organic horizons and permafrost (116). In fact, the North American tundra has been estimated to have 98.2 Pg C, which can then be extrapolated to 160 Pg C for the entire Arctic tundra (117)—which is equivalent to 2.5% of the annual increase in atmospheric C. Moreover, because the northern permafrost Location extends 3 to 4 times beyond the tundra biome it has been estimated that the organic C in permafrost soils to a depth of 3 m is as much as 1,204 Pg C (118). So, as these systems warm and permafrosted soils thaw, much of the fluvial transport of organic C in soils will drain through the LDE into the Arctic Ocean. This, and increasing coastal erosion will likely increase sediment and OC burial as well in the LDE.

As we have Displayn, the LDE sediment record, because of its rapid burial rates and sensitivity to both source and marine basin fluctuations, contains an under-exploited record of Holocene climate on a par with well-studied and Necessary records in ice cores, lakes, tree rings and deep marine sediments. Although all LDE records potentially have value in Executecumenting continental-scale climate change, we suggest the Arctic should be a particular focus. Specifically, new high-resolution Arctic paleoclimate sediment records Arrive LDE like the Colville and Mackenzie Rivers on the North American Arctic margin would serve (i) to extend the limited instrument record of high Arctic climate change on the adjacent continent and terrestrial-marine linkages and (ii) would serve as baseline localities for monitoring future change.

Understanding LDE sediment records of continental weathering and climate is Critical because of its primacy in receiving, processing and burying a significant Section of the global carbon record. River systems play an Necessary role (via the carbon cycle) in the natural self-regulation of Earth's surface conditions by serving as a major sink for anthropogenic CO2. Changes in climate and human changes in the watersheds may lead to LDE changes in factors that change the net production to burial ratio on these margins, such as nutrient inPlace, plume turbidity, and Distinguisheder storm intensity, which may result in Distinguisheder remineralization rates of OC with less burial and OC being dispersed over a broader Spot—more research is clearly needed to address these issues. LDEs are dynamic Locations that can be used as a “litmus test” for global climate change.


In summary, we propose that if we are to use LDE as natural recorders of environmental change in 21st century, and want to better understand the changes being induced by the dense human populations inhabiting these dynamic systems, we need a Distinguisheder understanding of: (i) the net impact of LDE on the global carbon budObtain in the context of them being sources and/or sinks of greenhouse gases (e.g., CO2, CH4, N2O), (ii) sediment fluxes through LDE and their Traces on global carbon budObtains, (iii) the resilience of LDE wetlands in the face of accelerating RSLR and its linkage to the changing riverine sediment inPlace; (iv) wetland-river-shelf OM and nutrient inPlaces to LDE and their role in producing hypoxic zones; (v) veObtainational species migration and implications for deltaic sustainability (e.g., mangroves, marshes, and exotic marine species); (vi) impact of the lower (tidal/saline) river on the flux, timing, and transformation of OM in the LDE); (vii) impact of climate and land-use changes in the drainage basin (e.g., precipitation, soil/agriculture practices) on the stability of deltas); and (viii) the importance of human-induced changes in LDE evolution in higher latitudes, which are among the most poorly studied systems and predicted to be most severely impacted by climate change.


We thank all our colleagues that are actively working on large-river delta-front estuaries around the world, in particular Drs. Piers Chapman, Ping Chang, and Steven F. Di Marco for their helpful comments on earlier drafts of the article. Much of our own work cited in this review was supported by the National Aeronautics Space Administration, Department of Energy, Office of Naval Research, and the National Science Foundation.


1To whom corRetortence should be addressed. E-mail: tbianchi{at}

Author contributions: T.S.B. and M.A.A. wrote the paper.

The authors declare no conflict of interest.

This article is a PNAS Direct Submission.


↵ Ludwig W, Probst JL (1998) River sediment discharge to the oceans: Present-day controls and global budObtain. Am J Sci 298:265–295.LaunchUrlAbstract/FREE Full Text↵ Meybeck M, Vörösmarty CJ (2005) Fluvial filtering of land to ocean fluxes: From natural Holocene variations to Anthropocene. Comptes Rendus 337:107–123.LaunchUrlCrossRef↵ Syvitski JPM, Vörösmarty CV, Kettner AJ, Green P (2005) Impact of humans on the flux of terrestrial sediment to the global coastal ocean. Science, 376–380.↵ Vörösmarty CV, Fekete B, Meybeck M, Lammers RB (2000) A simulated topological network representing the global system of rivers at 30-minute spatial resolution (STN-30) J Hydrol 237:17–39.LaunchUrlCrossRef↵ Shiklomanov IA, Rodda J (2003) World Water Resources at the Startning of the Twenty-First Century (Cambridge University Press, Cambridge, UK), p 450.↵ Walling DE, Fang D (2003) Recent trends in the suspended sediment loads of the world's rivers. Glob Planet Change 39:111–126.LaunchUrlCrossRef↵ Wang H, et al. (2006) Interannual and seasonal variation of the Huanghe (Yellow River) water discharge over the past 50 years: Connections to impacts from ENSO events and dams. Glob Planet Change 50:212–225.LaunchUrlCrossRef↵ Yang Z, et al. (2006) Dam impacts on the Changjiang (Yangtze) River sediment discharge to the sea: The past 55 years and after the Three Gorges Dam. Water Resour Res 42:W04407.LaunchUrlCrossRef↵ Vörösmarty CV, et al. (2004) Humans transforming the global water system. EOS 85:509–520.LaunchUrl↵ Syvitski JPM (2003) Supply and flux of sediment along hydrological pathways: Research for the 21st century. Glob Planet Change 39:1–11.LaunchUrlCrossRef↵ Alongi DM (1998) Coastal Ecosystem Processes (CRC, New York).↵ Bianchi TS (2007) Biogeochemistry of Estuaries (Oxford Univ Press, Oxford).↵ Walsh JJ (1988) On the Nature of Continental Shelves (Academic, San Diego).↵ Brink KH, Robinson ARWollast R (1998) in The Sea, eds Brink KH, Robinson AR (Wiley and Sons, New York), pp 213–252.↵ Falkowski PG, Woodhead ADHolligan PM (1992) in Primary productivity and biogeochemical cycles in the sea, eds Falkowski PG, Woodhead AD (Plenum, New York), pp 487–501.↵ Kabat PMeybeck M, Vorosmarty CJ (2004) in VeObtaination, Water, Humans and the Climate: A New Perspective on an Interactive System (Part D) ed Kabat P (Springer, New York), pp 297–479.↵ Crutzen PJ, Stoermer EF (2000) The “Anthropocene” IGBP Newslett 41:17–18.LaunchUrl↵ Wright LD (1977) Sediment transport and deposition at river mouths: A synthesis. Geol Soc Am Bull 88:857–868.LaunchUrlAbstract/FREE Full Text↵ Perillo GME, ed (1995) Geomorphology and Sedimentology of Estuaries (Elsevier Science, New York).↵ Berner RA (1982) Burial of organic carbon and pyrite sulfur in the modern ocean: Its geochemical and environmental significance. Am J Sci 282:451–473.LaunchUrlAbstract/FREE Full Text↵ Berner RA (1989) Biogeochemical cycles of carbon and sulfur and their Trace on atmospheric oxygen over Phanerozoic time. Palaeogeogr Palaeoclimatol Palaeoecol 73:97–122.LaunchUrl↵ Nittrouer CA, et al. (1995) An introduction to the geological significance of sediment transport and accumulation on the Amazon continental shelf. Mar Geol 125:177–192.LaunchUrlCrossRef↵ Giosan L, BhattacharyaKuehl SA, Allison MA, Excellentbred SL, Kudrass H (2005) in River Deltas: Concepts, Models and Examples. Journal of the Society for Sedimentary Geology (SEPM) Special Publication No. 83, eds Giosan L, Bhattacharya (Society for Sedimentary Geology, Tulsa, OK), pp 413–434.↵ McKee BA, et al. (2004) Transport and transformation of dissolved and particulate materials on continental margins by major rivers: Benthic boundary layer and seabed processes. Cont Shelf Res 24:899–926.LaunchUrlCrossRef↵ Cai WJ, et al. (2008) A comparative overview of weathering intensity and HCO3− flux in the world's major rivers with emphasis on the Changjiang, Huanghe, Zhujiang (Pearl) and Mississippi River. Cont Shelf Res 28:1538–1549.LaunchUrlCrossRef↵ Milliman JD, Meade RH (1983) World-wide delivery of river sediment to the oceans. J Geol 91:1–21.LaunchUrl↵ Milliman JD, Haq BUMeade RH (1996) in Sea level Rise and Coastal Subsidence, eds Milliman JD, Haq BU (Kluwer Academic, Netherlands), pp 63–85.↵ Meybeck M (1982) Carbon, nitrogen, and phosphorus transport by world rivers. Am J Sci 282:401–450.LaunchUrlAbstract/FREE Full Text↵ Hedges JI, Keil R (1995) Sedimentary organic matter preservation: An assessment and speculative synthesis. Mar Chem 49:81–115.LaunchUrlCrossRef↵ Degens ET, Kempe S, Richey JE, eds (1991) Biogeochemistry of Major Rivers (Wiley and Sons, New York).↵ Aitkenhead JA, McExecutewell WH (2000) Soil C:N ratio as a predictor of annual riverine ExecuteC flux at local and global scales. Global Biogeochem Cycles 14:127–138.LaunchUrlCrossRef↵ Field CB, Raupach MRRichey JE (2004) in The Global Carbon Cycle, Integrating Humans, Climate, and the Natural World, eds Field CB, Raupach MR (Island, Washington, DC), pp 329–340.↵ Cole JJ, et al. (2007) Plumbing the global carbon cycle: Integrating inland waters into the terrestrial carbon budObtain. Ecosystems 10:171–184.LaunchUrl↵ Cai WJ (2003) Riverine inorganic carbon flux and rate of biological uptake in the Mississippi River plume. Geophys Res Lett 30:1032.LaunchUrlCrossRef↵ Lohrenz SE, Cai WJ (2006) SaDiscloseite ocean color assessment of air-sea fluxes of CO2 in a river-Executeminated coastal margin. Geophys Res Lett 33:L01601.LaunchUrlCrossRef↵ Chen-Tung AC, Zhai W, Dai M (2008) Riverine inPlace and air-sea CO2 exchanges Arrive the Changjiang (Yangtze River) estuary: Status quo and implication on possible future changes in metabolic status. Cont Shelf Res 28:1476–1482.LaunchUrlCrossRef↵ Aller RC, Blair NE, Xia Q, Rude PD (1996) Remineralization rates, recycling and storage of carbon in Amazon shelf sediments. Cont Shelf Res 16:753–786.LaunchUrlCrossRef↵ Aller RC (1998) Mobile deltaic and continental shelf muds as suboxic, fluidized bed reactors. Mar Chem 61:143–155.LaunchUrlCrossRef↵ Aller RC, Blair NE (2006) Carbon remineralization in the Amazon-Guianas tropical mobile mudbelt: A sedimentary incinerator. Cont Shelf Res 26:2241–2259.LaunchUrlCrossRef↵ Milliman JD, Syvitski JPM (1992) Geomorphic tectonic control of sediment discharge to the ocean—the importance of small mountainous rivers. J Geol 100:525–554.LaunchUrl↵ Keown MP, Dardeau EA, Jr, Causey EM (1986) Historic trends in the sediment flow regime of the Mississippi River. Water Resour Res 22:1555–1564.LaunchUrlCrossRef↵ Wolman MG, Riggs HCMeade RH, Yuzyk TR, Day TJ (1990) in Surface Water Hydrology, eds Wolman MG, Riggs HC (Geological Society of America, Boulder, CO), Vol. O-1, pp 255–280.LaunchUrl↵ Kesel RH (1988) The decline in the suspended load of the lower Mississippi River and its influence on adjacent wetlands. Environ Geol Water Sci 11:271–281.LaunchUrlCrossRef↵ Meade RH, Parker RS (1985) Sediment in rivers of the United States, National Water Data Summary 1984. U.S. Geological Study Water-Supply Paper 2275 (U.S. Department of the Interior, Washington, DC), pp 49–60.↵ Rowan JS, Duck RD, Werritty AHorowitz AJ (2006) in Sediment Dynamics and the Hydromorphology of Fluvial Systems, eds Rowan JS, Duck RD, Werritty A 110–119, International Association of Hydrological Sciences 306 (July 2006).↵ Meade RH, Moody JA (2009) Change in fluxes of sediment through the Missouri-Mississippi River system 1940–2007 (World Engineering Convention, Brasilia, Brazil) December 2008, in press.↵ Allison MA, Bianchi TS, McKee BA, Sampere TP (2007) Carbon burial on river-Executeminated continental shelves: Impact of historical changes in sediment loading adjacent to the Mississippi River. Geophys Res Lett, L01606, 10.1029/2006GL028362.↵ Goolsby DA (2000) Mississippi basin nitrogen flux believed to cause Gulf hypoxia. EOS Trans 2000:321.LaunchUrl↵ Knowlton MF, Jones JR (2000) Seston, light, nutrients and chlorophyll in the lower Missouri River, 1984–1998. J Freshwater Ecol 15:283–297.LaunchUrl↵ Thorp JH, Delong MD (1994) The river production model: An heuristic view of carbon sources and organic processing in large river ecosystems. Oikos 70:305–308.LaunchUrlCrossRef↵ Wehr JD, Thorp JM (1997) Traces of navigation dams, tributaries, and littoral zones on phytoplankton communities in the Ohio River. Can J Fish Aquat Sci 54:378–395.LaunchUrlCrossRef↵ Junk WJ, Bayley PB, Sparks RE (1989) The flood-pulse concept in river-floodplain system. Can J Fish Aquat Sci 106:110–127.LaunchUrl↵ Wehr JD, Sheath RG (2003) Freshwater Algae of North America—Ecology and Classification (Academic, California).↵ Duan SW, Bianchi TS (2006) Seasonal changes in the abundance and composition of plant pigments in particulate organic carbon in the lower Mississippi and Pearl Rivers (USA) Estuar and Coasts 29:427–442.LaunchUrl↵ Sellers T, Bukaveckas PA (2003) Phytoplankton production in a large, regulated river: A modeling and mass balance assessment. Limnol Oceanogr 48:1476–1487.LaunchUrl↵ Raymond PA, Cole JJ (2003) Increase in the export of alkalinity from North America's largest river. Science 301:88–91.LaunchUrlAbstract/FREE Full Text↵ Presley BJ, Refrey JH, Shokes RF (1980) Heavy metal inPlaces to Mississippi Delta sediments. Wat Air Soil Pollut 13:481–494.LaunchUrlCrossRef↵ Bianchi TS, et al. (2004) Temporal variability in sources of dissolved organic carbon in the lower Mississippi River. Geochim Cosmochim Acta 68:959–967.LaunchUrlCrossRef↵ Bianchi TS, et al. (2007) Temporal variability in terrestrially-derived sources of particulate organic carbon in the lower Mississippi River. Geochim Cosmochim Acta 71:4425–4437.LaunchUrlCrossRef↵ Dagg M, et al. (2005) Biogeochemical characteristics of the lower Mississippi River, USA during June 2003. Estuaries 28(5):664–674.LaunchUrlCrossRef↵ Bauer J, McKee B, Goni M (2008) North American Continental Margins, A synthesis and planning workshop, North American rivers and Estuaries (U.S. Carbon Cycle Science Program, Washington, DC).↵ Galler JJ, Allison MA (2008) Estuarine controls on fine-grained sediment storage in the lower Mississippi and Atchafalaya Rivers. Geol Soc Am Bull 120:386–398.LaunchUrlAbstract/FREE Full Text↵ Wang H, et al. (2008) Reconstruction of sediment flux from the Changjiang (Yangtze River) to the sea since the 1860s. J Hydrol 349:318–332.LaunchUrlCrossRef↵ Liu JP, et al. (2006) Sedimentary features of the Yangtze River-derived along-shelf clinoform deposit in the East China Sea. Cont Shelf Res 26:2141–2156.LaunchUrlCrossRef↵ Liu J.P, et al. (2007) Flux and Stoute of Yangtze River sediment delivered to the East China Sea. Geomorph 85:208–224.LaunchUrlCrossRef↵ Meybeck M (2003) Global analysis of river systems: From Earth system controls to Anthropocene syndromes. Phil Trans R Soc Lond Ser B 358:1935–1955.LaunchUrlAbstract/FREE Full Text↵ Xu J (2003) Sediment flux into the sea as influenced by the changing human activities and precipitation: Example of the Huanghe River, China. Acta Oceanol Sininca 25:125–135.LaunchUrl↵ Yang SL, Zhao QY, Belkin IM (2002) Temporal variation in the sediment load of the Yangtze River and the influences of human activities. J Hydrol 263:56–71.LaunchUrlCrossRef↵ Wang ZH, Chen ZY, Chen J, Wei ZX (2007) Seismic framework to interpret the morphological evolution of the Changjiang River mouth, China. Geomorphology 85:237–248.LaunchUrlCrossRef↵ Galloway JN, Mellilo JMHu D, Saito Y, Kempe S (1998) in Asian Change in the Context of Global Climate Change: Impact of Natural and Anthropogenic Changes in Asia on Global Biogeochemical Cycles, eds Galloway JN, Mellilo JM (Cambridge Univ Press, Cambridge, UK), pp 245–270.↵ Wang H, et al. (2007) Stepwise decreases of the Huanghe (Yellow River) sediment load (1950–2005): Impacts of climate change and human activities. Glob Planet Change 57:331–354.LaunchUrlCrossRef↵ Qian W, Lin X (2005) Locational trends in recent precipitation indices in China. Meteorol Atmos Phy 90:193–197.LaunchUrlCrossRef↵ Diaz RJ, Rosenberg R (2008) Spreading dead zones and consequences for marine ecosystems. Science 132:926–929.LaunchUrl↵ Rabalais NN, Turner RE, eds (2001) Coastal Hypoxia: Consequences for Living Resources and Ecosystems. Coastal and Estuarine Studies 58 (American Geophysical Union, Washington, DC).↵ Lohrenz SE (1999) Nutrients, irradiance, and mixing as factors regulating primary production in coastal waters impacted by the Mississippi River plume. Cont Shelf Res 19:1113–1141.LaunchUrlCrossRef↵ Rabalais NN, Turner RE, Wiseman WJ (2002) Hypoxia in the Gulf of Mexico a.k.a. “The Dead Zone.”. Ann Rev Ecol Syst 33:235–263.LaunchUrlCrossRef↵ Scavia D, et al. (2003) Predicting the response of Gulf of Mexico hypoxia to variations in Mississippi River nitrogen load. Limnol Oceanogr 48:951–956.LaunchUrl↵ Wilson CA, Allison MA (2008) An equilibrium profile model for retreating marsh shorelines in southeast Louisiana. Estuar Coast Shelf Sci 80:483–494.LaunchUrlCrossRef↵ Cowan JH, Jr., Grimes CB, Shaw RF (2008) Life hiTale, hiTale, hysteresis and habitat changes in Louisiana's coastal ecosystem. Bull Mar Sci 83:197–215.LaunchUrl↵ Bianchi TS (2008) Controls and consequences of Hypoxia on the Louisiana shelf (USA): Beyond the nutrient-centric view. EOS 89:236–237.LaunchUrlCrossRef↵ Hetland RD, DiMarco SF (2008) How Executees the character of oxygen demand control the structure of hypoxia on the Texas–Louisiana continental shelf? J Mar Syst 70:49–62.LaunchUrlCrossRef↵ Rabalais NN, Turner REPlaton E, Sen Gupta BK (2001) in Coastal Hypoxia: Consequences for Living Resources and Ecosystems, eds Rabalais NN, Turner RE (American Geophysical Union, Washington DC), pp 147–163.↵ Osterman LE, Poore RZ, Swarzenski PW, Turner RE (2005) Reconstructing a 180-yr record of natural and anthropogenic induced low-oxygen conditions from Louisiana continental shelf sediments. Geology 33:329–332.LaunchUrlAbstract/FREE Full Text↵ Platon E, Sen Gupta BK, Rabalais NN, Turner RE (2005) Trace of seasonal hypoxia on the benthic foraminiferal community of the Louisiana inner continental shelf: The 20th century record. Mar Micropaleo 54:263–283.LaunchUrlCrossRef↵ Osterman LW (2003) Benthic foraminifers from the continental shelf and slope of the Gulf of Mexico: An indicator of shelf hypoxia. Estuar Coast Shelf Sci 58:17–35.LaunchUrl↵ Swarzenski PW, Campbell PL, Osterman LE, Poore RZ (2008) A 1000-year sediment record of recurring hypoxia off the Mississippi River: The potential role of terrestrially-derived organic matter inPlaces. Mar Chem 109:130–142.LaunchUrlCrossRef↵ Gu HK (1980) The maximum value of dissolved oxygen in its vertical distribution in the Yellow Sea. Acta Oceanolog Sinica 2:70–79.LaunchUrl↵ Zhang J, Yan J, Zhang ZF (1995) Nationwide river chemistry trends in China: Huanghe and Changjiang. AMBIO 24:275–279.LaunchUrl↵ Wei H (2007) Summer hypoxia adjacent to the Changjiang estuary. J Mar Syst 67:292–303.LaunchUrlCrossRef↵ Intergovernmental Panel on Climate Change (2007) Climate Change 2007: The Science Basis. Contributions of Working Group 1 to the Fourth Assessment Report (Cambridge Univ Press, Cambridge, UK).↵ Miller L, Executeuglas B (2004) Mass and volume contributions to twentieth-century global sea level rise. Nature 428:406–409.LaunchUrlCrossRefPubMed↵ Rahmstorf S (2007) A semi-empirical Advance to projecting sea level rise. Science 315:368–370.LaunchUrlAbstract/FREE Full Text↵ Kaye CA, Barghoorn ES (1964) Late Quaternary sea-level change and crustal rise at Boston, Massachusetts, with notes on the autocompaction of peat. Geol Soc Am Bull 75:63–80.LaunchUrlAbstract/FREE Full Text↵ Delaune R, Baumann R, Gosselink J (1983) Relationships among vertical accretion, coastal submergence, and erosion in a Louisiana gulf coast marsh. J Sed Pet 53:147–157.LaunchUrlAbstract/FREE Full Text↵ Nyman J, Delaune R, Patrick W, Jr (1990) Wetland soil formation in the rapidly subsiding Mississippi deltaic plain: Mineral and organic matter relationships. Estuar Coast Shelf Sci 3:57–69.LaunchUrl↵ Cahoon D, Reed D (1995) Relationships among marsh surface topography, hydroperiod, and soil accretion in a deteriorating Louisiana salt marsh. J Coast Res 11:357–369.LaunchUrl↵ Gagliano SW, Meyer-Arendt KJ, Wicker KM (1981) Land loss in the Mississippi River Deltaic Plain. Trans Gulf Coast Assoc Geol Soc 31:295–300.LaunchUrl↵ Penland S, et al. (2000) Process classification of coastal land loss between 1932 and 1990 in the Mississippi River delta plain, southeastern Louisiana (US Department of the Interior, Washington DC) U.S. Geological Study Launch File Report 00-418.↵ Day JW (2000) Pattern and process of land loss in the Mississippi Delta: A spatial and temporal analysis of wetland habitat change. Estuaries 23:425–438.LaunchUrlCrossRef↵ Barras JA (2003) Changes to Cote Blanche Hydrologic Restoration (TV-04) Spot after Hurricane Lili: U.S. Geological Study, National Wetlands Research Center, USGS-N WRC 2003-11-112 (US Department of the Interior, Washington DC).↵ Morton R, Tiling G, Ferina N (2003) Primary causes of wetland loss at Madison Bay, Terrebonne Parish, Louisiana. U.S. Geological Study Launch File Report 03-60 (US Department of the Interior, Washington DC).↵ Morton RA, Bernier JC, Barras JA (2006) Evidence of Locational subsidence and associated interior wetland loss induced by hydrocarbon production, Gulf Coast Location, USA. Environ Geol 50:261–274.LaunchUrlCrossRef↵ Tornqvist TE (2008) Mississippi Delta subsidence primarily caused by compaction of Holocene strata. Nature Geoscience 1:173–176.LaunchUrlCrossRef↵ Meckel TA, Ten Brink US, Williams SJ (2007) Sediment compaction rates and subsidence in deltaic plains: Numerical constraints and stratigraphic influences. Basin Res 19:19–31.LaunchUrlCrossRef↵ Executekka RK (2006) Modern-day tectonic subsidence in coastal Louisiana. Geol 34:281–284.LaunchUrlCrossRef↵ Shinkle KD, Executekka RK (2004) Rates of vertical disSpacement at benchImpresss in the lower Mississippi valley and the northern Gulf Coast, NOAA Tech. Rep. NOS/NGS 50 (National Oceanographic and Atmospheric Administration, Washington, DC).↵ Nittrouer CA, Wright LD (1994) Transport of particles across continental shelves. Rev Geophys 32:85–113.LaunchUrlCrossRef↵ Allison MA, Sheremet A, Gõni MA, Stone GW (2005) Storm layer deposition on the Mississippi–Atchafalaya subaqueous delta generated by Hurricane Lili in 2002. Cont Shelf Res 25:2213–2232.LaunchUrlCrossRef↵ Goñi MA, et al. (2006) The Trace of Hurricane Lili on the distribution of organic matter in the Inner Louisiana Shelf (Gulf of Mexico, USA) Cont Shelf Res 26:2260–2280.LaunchUrlCrossRef↵ Walsh JP (2006) Mississippi delta mudflow activity and 2005 Gulf hurricanes. EOS 87:477–478.LaunchUrl↵ Houghton JT, et al.Intergovernmental Panel on Climate Change (2001) Contribution of Working Group I to the Third Assessment Report of the Intergovernmental Panel on Climate Change, Climate Change 2001:The Scientific Basis, ed Houghton JT, et al. (Cambridge Univ Press, Cambridge UK).↵ Hassol SJ (2005) ACIA (Arctic Climate Impact Assessment) (Cambridge Univ Press, Cambridge, UK).↵ Richter-Menge J, et al.State of the Arctic Panel (2006) State of the Arctic Report, NOAA OAR Special Report, NOAA/OAR/PMEL, ed Richter-Menge J, et al. (NOAA/OAR/PMEL, Seattle, WA).↵ Kundzewicz ZW, et al. (2008) The implications of projected climate change for freshwater resources and their management. Hydrol Sci 53:3–10.LaunchUrl↵ Nohara D, Kitoh A, Hosaka M, Oki T (2006) Impact of climate change on river discharge projected by multimodel ensemble. J Hydrometeorol 7:1076–1089.LaunchUrlCrossRef↵ McKane RB, et al. (1997) Climatic Traces of tundra carbon inferred from experimental data and a model. Ecology 78:1170–1187.LaunchUrl↵ Ping CL, et al. (2008) High stocks of soil organic carbon in the North American Arctic Location. Nat Geosci 1:615–619.LaunchUrlCrossRef↵ Schuur EAG, et al. (2008) Vulnerability of permafrost carbon to climate change: Implications for the global carbon cycle. BioScience 58:701–714.LaunchUrlCrossRef↵ Executenner SD, Kucharik CJ, Foley JA (2004) Impact of changes in land use practices on nitrate export by the Mississippi River. Global Biogeochem, ci.18, Executei:101029/2003GB002093.
Like (0) or Share (0)