Climate Program Office
Natural Storm Variability in New England part of Vignettes:Vignette Collection
Why storms? Climate is the long-term average of variables in the Earth's atmosphere, such as temperature, precipitation, and wind. For millions of years, climatic events, such as rainstorms, have shaped the earth's surface leaving sediment deposits that can be studied to understand climate. By compiling pre-historic, sedimentary records, researchers can define natural climate patterns as well as variations that could have detrimental effects to society (i.e. climate change). Understanding the natural variability in precipitation, for example, is necessary for distinguishing and projecting changes that may accompany climate change. Decreases in the frequency and magnitude of rainstorms could cause drought that destroys crops and threatens drinking water supply. Conversely, an increase in the frequency or magnitude of rainfall could cause floods that damage development, stress critical infrastructure such as roads and storm drains, and more importantly endanger lives. Thus, deciphering geomorphic records of precipitation and damaging floods preserved in natural archives enables society to understand and plan for floods of the future. In the heavily populated northeastern United States, big rainstorms are known to have caused floods that significantly changed the landscape and damaged developed areas. Sedimentary records of these events are preserved in lakes and along valley floors through New York, Vermont, New Hampshire, and Maine (Figure 1). For this reason, New England is an apt setting for undertaking geomorphic research on climate variability. What is the evidence of storms? The upper reaches of watersheds in New England commonly consist of steep hillslopes with loose sediment including fine silts and sands as well as coarse gravel, cobbles, and boulders. During storms, rainfall collects in narrow depressions on the hillslope (gullies) and accelerates as it moves downhill, initiating erosion of the sediment on the hillside. At the base of the hillslope, water dissipates across the valley floor, depositing sediment as the water decelerates. In these instances, the sediment forms a recognizable, cone-shaped deposit, called an alluvial fan. Backhoes can be used to dig trenches across alluvial fans, where geomorphologists distinguish storm deposits containing coarse sediment poorly mixed with silt, sand, and other debris (Figure 2). In other locations, rainfall collects in streams that flood during storms, eroding the stream channel. Across New England, many streams flow directly into lakes, forming deltas where coarse sediment settles in the lake and on the lake margin. The coarse sediment forms characteristic layers that contrast sharply with the fine-grained organic muds that slowly accumulate in lakes over time (Figure 3). These unique layered deposits can be studied by collecting sediment core samples from suitable lakes and analyzing the sediment in the cores using lab tests that identify key characteristics such as grain size (texture), organic content, and color. Hundreds of these flood-deposited layers have been documented in alluvial fan trenches and in sediment cores collected from lakes in New York, Vermont, New Hampshire, and Maine. After the positions of flood layers have been documented, radiocarbon dating methods are used to determine their ages. In a single sediment core sample or fan trench, numerous pieces of organic material are collected and dated: small pieces of charcoal and plant seeds, leaves, and stems are the most common materials that are dated in these deposits. The exact timing of these events, derived from the radiocarbon dates, is important primarily because it allows the record of storms revealed in a single lake or fan to be compared with those of other sites. Where these records are synchronized, it increases our scientific confidence that the storms were related to regional climate patterns as opposed to conditions specific to a single locality. For example, a local convective thunderstorm could initiate flooding in one lake watershed and leave neighboring watersheds dry. However, large storms, such as hurricanes and extra-tropical cyclones ("nor'easters"), would cause flooding across New England resulting in lake deposits and alluvial fans with the same or similar ages (Figure 4). What does the evidence say? Patterns of past storminess have been identified from the geomorphic records of both New England lakes and alluvial fans (Figure 4). These records indicate that over the past 12,000 years, when landscape looked similar to today, storm activity increased and decreased in the New England region several times (Figure 4). The record of storms from New York and Vermont lakes and alluvial fans reveal a consistent 3,000-year pattern where storms increase. The regional patterns revealed by both the sedimentary evidence and historical meteorological observations suggest long-term changes in the preferred state of the Arctic Oscillation as the likely synoptic-scale climate driver. However, this pattern is not evident in the record from New Hampshire and Maine. The discrepancy may reflect regionally distinct climatic processes, or a contrasting methodology used to analyze the cores from these two regions. Both sets of lake records show an increase in the frequency of storms over the past 4,000 years, as well as a distinct period of increased storminess around 6,000 years ago. Because there is agreement between the records throughout New England over the more recent period, a regional climate pattern of increased storminess may be emerging. The lake records also suggest that storminess is continuing to increase towards the present day. Regional patterns of climate, such as those caused by the El Niño/Southern Oscillation, have significant impacts on people's lives in other localities. Further geomorphic research is necessary to ensure accurate comparison between the lake and alluvial fan records and to distinguish natural patterns of storms in the New England region.
Sea Level Rise in the San Francisco Bay Considering Morphology in Adapting Management part of Vignettes:Vignette Collection
The San Francisco Bay A Community Investment The San Francisco Bay (Bay) is part of the largest estuary on the west coast of North America. It supports a densely populated and prosperous surrounding cultural landscape (Figure 1). In combination with the contiguous Sacramento-San Joaquin Delta, the estuary historically covered over 800,000 acres (3,000 km²) supporting diverse natural habitats including open waters, tidal flats, and freshwater, brackish, and saline tidal wetlands (Goals Project 1999). One of the most unique aspects of the San Francisco Bay area population is that, after a period of widespread development eliminated over 80% of the tidal wetlands from the 1850s to the late 1960s, the region made political and financial investments to conserve and, more recently, restore the Bay ecosystem. Projected rates of sea level rise over the next century now require a new management strategy to preserve that community investment, as well as to protect the huge financial investment in infrastructure and urban development (Parris and Lacko 2009). The Changing Morphology and Management of the San Francisco Bay Geomorphologic and other scientific studies of the San Francisco Bay chronicle a history of rising seas that have shaped and re-shaped the Bay bottom and shoreline. Sediment cores tell us that the Bay formed during a period of rapid sea level rise, spurred by warming temperatures and melting glaciers, starting about 10,000 years ago and lasting about 6,000 years (Atwater et al. 1979, Byrne et al 2001, Malamud-Roam et al 2007, Watson 2004). Geomorphic analysis of historical evidence from the late 1800s (navigation charts, topographic surveys, maps from Spanish settlers, etc) and sediment coring studies demonstrate how the continual motion of the tides gradually shaped the Bay shoreline into a vast network of biologically diverse, densely-vegetated tidal marshes along the Bay shoreline (Figure 2). US Coast Survey navigation charts also provide the necessary data for bathymetric analysis of the underwater (subtidal) areas of the Bay, a revealing aspect of the morphologic history of the Bay (Jaffe and Foxgrover 2006, Jaffe et al 2007). As the Bay shoreline was being developed, surface mining in the Sacramento-San Joaquin watershed eroded vast amounts of fine sediment from the Sierran hillslopes which was then transported by the rivers and deposited in the Bay (McKee et al 2006, Jaffe et al 2007, Schoelhammer et al 2007). From the 1850s to the 1890s, more than 250,000,000 cubic yards (~191,138,715 cubic meters) of sediment was deposited in the Bay primarily from the Sacramento-San Joaquin watershed, enough to fill 60 Superdomes (Jaffe et al 2007, SFEI 2009). Some of this sediment was used by developers to "fill" tidal wetlands and shallow water areas of the Bay in preparation for building; additional sediment was dredged to deepen Bay channels for shipping and navigation. Comparison of the historic records and present day aerial photographs reveal that this unregulated development of the Bay and its shoreline eliminated 80% of the tidal marshes on the Bay shoreline (Figure 3) (Goals Project 1999). Since then, former and remaining wetlands have been utilized for development and managed for a variety of uses, including salt production, flood control, utility corridors, recreation, and, to an increasing extent, conservation. In the late 1960s, groundbreaking policy (the MacAteer-Petris Act) was passed in the California Legislature prohibiting un-permitted development by regulating the use of "fill" and securing the public right to access the Bay. This legislation formed the San Francisco Bay Conservation and Development Commission (BCDC) as a management agency that presently regulates and enforces Bay fill. With controls on development and community support for the environment, over $100 million dollars has been invested in restoring tidal marshes on the Bay shoreline. This investment includes the largest tidal marsh restoration project on the west coast (~16,500 acres or 67 km2), which is currently in progress in the South San Francisco Bay, and significant projects in San Pablo Bay. The Bay still retains critical wetlands for endangered species and other wildlife, and large areas could be restored elsewhere in the Bay. However, the fate of existing and future restoration efforts depends on the development of new policy and management paradigms to address projected increases in sea level rise (Parris and Lacko 2009). Erosion An Ecosystem Tipping Point Based on 30 years of restoration experience in the Bay, geomorphologists have demonstrated that, aside from available land, a major component of a successful restoration is the availability of a plentiful supply of fine sediment (Orr et al 2003, PWA and Faber 2004). Tidal marshes are able to adapt to sea-level rise by accretion and migration (collectively referred to as "retreat" or "transgression") (Figure 4). Accretion in tidal marshes is a combination of organic accumulation from decaying marsh plants and inorganic sediment deposition. Inorganic deposition occurs when waves erode sediment from tidal flats and low elevation tidal marshes and tides deposit that sediment onto the higher marsh or land newly restored to tidal action. As sea level rises, the tides reach further landward and inundate previously upland areas. In this fashion, tidal marshes migrate upward and landward as sea level rises. A combination of faster sea level rise, limited open space for restoration, less sediment coming into the Bay, and less sediment existing within the Bay could reduce the ability of marshes to accrete and migrate, causing erosion of tidal marshes and making future restoration more difficult (Callaway et al 2007, Orr et al 2003, Parris and Lacko 2009). In comparison to the historic periods, more sediment is now trapped behind water supply and flood control dams; dams also reduce flood flows, limiting the transport of the available sediment pool from the watershed to the Bay (McKee et al 2006, Jaffe et al 2007, Schoelhammer et al 2007). The Sacramento-San Joaquin watershed, once thought to be a source of approximately 90% of the sediment entering the bay, is now estimated to contribute only 60% of sediment inflow (McKee et al 2006). Local tributary watersheds, such as the Napa and Sonoma rivers and Alameda Creek, contribute the remaining 40%, but are not yet actively managed to direct valuable sediment supplies to desirable shoreline sites. The area of tidal flats in the Bay, an important source of sediment for the marshes, has been reduced by more than 60,000 acres (Jaffe and Foxgrover 2006, Jaffe et al 2007, SFEI 2009). If the rate of human-induced carbon dioxide emissions equals the past forty years, the United States Geological Survey (USGS) projects a rise in sea level of 46 centimeters (18 inches) by mid-century (2040-2060) and 140 centimeters (55 inches) by the end of the century (2090-2110) (Cayan et al 2008, Knowles and Cayan 2002, Knowles 2008). This amount of sea level rise would more than double the historic rate of sea level rise from approximately 0.1 inches per year to 0.3 inches per year, increasing the risk of erosion in the Bay and on the Bay shoreline. Erosion will lead to loss of tidal marshes and tidal flats, and it will also undermine the many protection structures (seawalls, rip-rap revetments, levees, etc) that separate residential and urban developments from flooding. In most cases, protection structures accelerate erosion (Griggs 2005). Seawalls and levees reflect wave energy back onto the adjacent shoreline. Construction and maintenance of these structures often requires the use of sediment, diminishing the sediment pool available for tidal restoration. Using these structures, the cost of protecting development alone against a 55-inch rise in sea level is estimated to be about $14 billion (Heberger et al 2008). Adaptation in the Bay New Management and Policy Widespread and continued erosion in the Bay and along the Bay shoreline could have devastating consequences for state of California and the southwestern United States. The Bay area is a center for innovation because it houses some of the world's leading universities, research institutions, and high-tech industries. Preserving and restoring tidal marshes and tidal flats may provide sustainable alternatives to structural protection, providing a natural buffer for valuable shoreline development. At the same time the impacts from existing and new structural protection will have to be offset by balancing ecosystem and development uses on the shoreline. The Bay ecosystem is a valuable nexus for preserving biodiversity, as a critical component of the Pacific Flyway, a nursery for native fisheries, and essential habitat for many species of special concern. This equitable management of the Bay requires new policies and management strategies for agencies like BCDC to honor the investment made by the Bay area community in the late 1960s for future generations to come.