Rediscovering, Reevaluating, and Restoring Lost River-Wetland Corridors

Introduction

We define a river-wetland corridor as a relatively wide valley floor within which there is space for persistent alluvial deposits and sufficient connectivity between surface and subsurface hydrology to create and maintain an interacting system of channels, wetlands, and floodplain ponds and lakes. Salient characteristics are that the water table is at or close to ground elevation much of the time, and the floodplain is inundated and/or saturated frequently and for long periods. This corridor always includes within it the active channel(s), geomorphic floodplain, underlying hyporheic aquifer, and associated riverine wetlands (Harvey and Gooseff, 2015). The corridor may occupy the entirety of an alluvial valley floor, or its extent may be limited naturally (e.g., by river terraces) or anthropogenically (e.g., by levees).

Our focus is on understanding river-wetland corridors at the reach scale. In this context, we define a reach of a river-wetland corridor as the length of contiguous alluvial valley between topographic or geological controls, within which the channel planform is laterally unconfined and free to adjust and evolve in response to the influences of stream flow, sediment load, large wood, vegetation, and animals (e.g., beaver (Castor spp.)). A reach may include more than one channel planform. Indeed, as noted by (Leopold and Wolman 1957, p. 169), “A given reach of river may exhibit both braiding and meandering. In fact, Russell (1954) points out that the Meander River in Turkey, which gave us the term “meandering,” has both braided and straight reaches.” River-wetland corridors are then, discrete reaches along river networks, with spatial boundaries defined by distinctive characteristics of valley morphology and hydrology. “River” here includes all sizes of naturally flowing bodies of water, from creeks and brooks to the largest lotic ecosystems. The active channels are flow paths confined by streambanks and/or natural levees (Hey, 1979). Stream flow in a river-wetland corridor may predominantly follow a single channel that may be straight or meandering, it may follow multi-threaded channels (we use this term to include anastomosing, anabranching, and braiding), or stream flow may be unchanneled, with net movement down-valley occurring via a diffuse and shifting network of preferential flow paths. The geomorphic floodplain is composed of layers of fluvially deposited sediment and organic matter and is inundated and/or saturated for varying timespans from continuously to frequently. The floodplain surface is not flat, being composed of natural levees, levee back-slopes, splay deposits, abandoned channels, ridge and swale topography, back swamps, and open water bodies (ponds and lakes). Fluvial wetlands in the river-wetland corridor include seasonally saturated and inundated areas that may be linked to stream channels via surface (rheic) connections, subsurface (hyporheic) connection, or both (Ward, 1989; Stanford and Ward, 1993; Petts and Amoros, 1996). River-wetland corridors are, like the floodplains within which they exist, built and maintained by net deposition of sediment. That said, although dynamic adjustments of the river-wetland corridor are led by deposition, sediment erosion, transport, and exchange processes also play significant roles. Rates of net sedimentation may be imperceptible or matched by those of sediment compaction and floodplain subsidence, so that river-wetland corridors adjust continually over timespans of years to decades. We refer to this scenario as being dynamically stable in that the fundamental characteristics of abundant wetlands and substantial channel-floodplain hydrologic connectivity persist, although the detailed morphology of the river corridor is continually adjusting to and accommodating inputs of water and sediment, and internal feedbacks with biota. Conversely, a river-wetland corridor cannot long persist if its river is actively incising (Cluer and Thorne, 2014).

River-wetland corridors are fundamentally groundwater-dependent (Boulton, 2005). Subsurface water may be derived from influent flow from the river (especially during floods), infiltration of local precipitation and surface water, or percolation from the regional aquifer (Loheide et al., 2009). This range of recharge sources is important because a characteristic attribute of river-wetland corridors is that they can maintain their wetlands through inflow and infiltration, even in the absence of inputs from regional aquifers (Melly et al., 2017). Recognizing this, a river-wetland corridor can be described as rheos (from the Greek rhéos—which translates as “stream”) in that it constantly exchanges water with, and is therefore part of, the river. The point here is that not all of the river (rheos) flows above ground. The part of the river that flows beneath the ground is the hypo-rheos (literally, the river below); hence, we refer to the alluvial aquifer as being hyporheic, in that it is characterized by flow paths that originate from, and terminate in, the river corridor above (Gooseff, 2010). Laterally beyond and vertically beneath the hyporheic aquifer is the perirheic zone, which is the domain of water that is not part of the river, being sourced from and exchanged with that in other systems, such as valley side-slope hydrology and regional groundwater (Mertes, 1997) (Figure 1).

FIGURE 1

FIGURE 1. Examples of “contemporary remnants” in which fully functional river-wetland corridors still exist: (A) Pantanal, River Paraguay, Brazil; (B) Okavango Delta, Okavango River, Botswana; (C) The Gearagh, River Lee, Ireland; (D) North St. Vrain Creek, Colorado, United States. Each scale bar is approximately 300 m long.

River-wetland corridors can be laterally expansive and tend to be longitudinally discontinuous, alternating downstream with other river corridor configurations (e.g., relatively steep, laterally confined reaches) as valley geometry and/or fluxes into and out of the river corridor vary through space and time. River-wetland corridors can develop throughout the drainage network, from small, headwater streams in which meadows cover fractions of a hectare, to the lowermost courses and deltas of major rivers that drain basins with areas of thousands of square kilometers (e.g., the wet grasslands of the Florida Everglades or (historically) the bottomland forests and wood-dominated channels around the “Great Raft” on Louisiana’s Red River (Triska, 1984)).

Some areas of river-wetland corridors are perennially inundated, with aquatic vegetation ranging from algae to aquatic macrophytes. Larger areas are seasonally inundated and/or saturated, supporting a wide variety of wetland obligate, facultative, and riparian vegetation types including, but not limited to, woody species such as cottonwoods (Populus spp.), alder (Alnus spp.), and willows (Salix spp.), as well as sedges (Cyperaceae), rushes (Juncaceae), and grasses (Gramineae). Our definition of a river-wetland corridor thus subsumes beaver-meadows, riverine carr (a type of wetland dominated by shrubs; Whittow, 1984), sloughs, swamps, muskeg, bottomland forests (e.g., the várzea and igapó of the Amazon basin), wet meadows, wet woodlands, bosques (gallery forests), sausals, and ciénega (wetlands in the arid United States Southwest), along with open water ponds and lakes. A characteristic of all these vegetation assemblages is that plant cover in river-wetland corridors is typically dense, which contributes to sediment deposition and relatively high vegetative resistance to flow and fluvial erosion.

We conceptualize river-wetland corridors as falling on a continuum of types of river reach that form in valley segments with less lateral confinement and a lower gradient relative to reaches up- and downstream in the river network (Figure 2). The continuum of river types that extends from relatively dry, braided stream corridors to perennially wet river-wetland corridors is one of increasing hydrologic connectivity and complexity when integrated across three dimensions: longitudinally along the channel(s) and floodplain; vertically between the surface and subsurface components of river flow, and laterally between the channel, wetlands, floodplain, the valley sides, and adjacent uplands.

FIGURE 2

FIGURE 2. A schematic illustration of the continuum of channel planform, vegetation communities, and floodplain water table within wide, low-gradient valley segments. Inset illustrations are (1) Park Creek, MT, United States, (2) Harris Wash, UT, United States, (3) Swan River, MT, United States (4) bottomland hardwood forest along the Illinois River, IL, United States, (5) igapo forest, Amazon River, Brazil, (6) várzea forest on the Amazon River floodplain, Brazil, (7) wet meadow and lake, Yukon River, Alaska, United States (8) swamp on the floodplain of the Congaree River, SC, United States, (9) muskeg along the floodplain of the Yukon River, AK, United States, (10) an abandoned beaver pond in a wet-meadow stream corridor, CO, United States, and (11) wet-meadow stream corridor at Deep Creek, OR, United States.

In a river-wetland corridor, downstream passage of water, sediment, and organic material (e.g., large wood, detritus) is slowed due to lack of lateral confinement (resulting in wider, shallower flows), coupled with high flow resistance and permeable, in-channel obstructions (e.g., vegetation, logjams, beaver dams). This is especially the case in multi-threaded rivers, where the absence of a single, large, high-conveyance channel both reflects and enhances natural tendencies for sediment deposition and large wood retention. In essence, modulated longitudinal stream connectivity results in longer residence times for water, solutes, sediment, and organic matter in river-wetland corridors compared to river types with more concentrated flow paths and less spatial heterogeneity (Helton et al., 2014; Wohl, 2017).

Wide valley floors provide space for laterally extensive floodplains and channel migration zones that accommodate the full spectrum of channel planforms including straight, meandering, and multi-threaded (braided, anastomosing, anabranching). Braided rivers typically form where stream bank resistance to erosion is low compared to that of the stream bed; channel and valley gradients are relatively steep; and discharges relative to size of material in the channel (i.e., dimensionless discharges) are comparatively high (Eaton et al., 2010). Braided rivers can form in both wet and dry climates. A braided river floodplain can be well drained because of high hydraulic conductivity in the coarse sediment in which the floodplain is formed, or the floodplain can be sufficiently wet to fit our criteria for a river-wetland corridor. As the content of fine, cohesive sediment in floodplain soils increases and/or dense vegetation colonizes the riparian zone, the erosional resistance of stream banks increases. Both field observation (e.g., Schumm, 1985) and laboratory experimentation (e.g., Tal and Paola, 2010) show that cohesive soils and vegetation can transform a braided channel planform into one characterized by elements of meandering, anastomosing, and/or anabranching.

To provide context for current river-wetland corridor management and restoration efforts, we start by reviewing the historical and paleoenvironmental evidence of their past abundance and ubiquity and documenting their dramatic decline over the last two centuries. We examine the temporally and spatially dynamic roles of geology, biology, and geomorphology in their formation and persistence, and elucidate our characterization of polydimensional river-wetland corridors as “kaleidoscope rivers.” We close by establishing the functional significance of river-wetland corridors and consider the implications of their rediscovery for river restoration. We conclude that river-wetland corridors: 1) were wetter, more abundant, and widespread globally prior to intensive human alteration of catchments, valley floors, and channels; 2) support river functions that are compromised or lost when river-wetland corridors are simplified, degraded, or drained; and 3) should be both conserved through sustainable river management and recognized as a potentially legitimate and desirable target condition for river restoration that is necessary for the recovery of wetland obligate species as well as species that derive benefits from wetlands.

Former Abundance

Evidence of the antiquity, former abundance, and widespread distribution of river-wetland corridors exists in geological, paleoenvironmental, archeological, and historical records. For example, stratigraphy indicative of deposition by rivers with anastomosing or anabranching planforms suggests that rivers of this type began replacing braided rivers during the middle Devonian, ∼400 million years B.P. Coincidence between planform metamorphosis and colonization of river valleys by forests led (Davies and Gibling, 2011, p. 629) to conclude that, “…expansion of tree habitats led to the crossing of a threshold in vegetative control of floodplain and river morphology”. Paleoenvironmental information in the form of buried hydrosols, wetland plant macrofossils, and pollen (e.g., Brown, 2002; Davis et al., 2002) confirms that heavily vegetated, multi-threaded systems were much wetter than the contemporary, artificially drained river corridors to which we have become accustomed.

Archeological records are also useful for inferring the former existence of river-wetland corridors because people have settled near the rich resources of this valley type for millennia (e.g., Coles and Orme, 1983; Coles, 2000; Kim et al., 2008). Interpretations of several archeological sites in the United Kingdom, for example, suggest that some prehistoric human groups preferentially settled in valleys modified by beavers in order to exploit the fertile wet-meadows for grazing and cropland, re-use beaver-cut timber in building houses, and take advantage of abundant fish stocks (Liarsou, 2013).

Historical records in the form of photographs, maps (e.g., Kaatz, 1955; Hohensinner et al., 2021), written descriptions (e.g., Christy and Alverson, 2011), place names (Brown et al., 2018), and drawings provide evidence of the more recent existence of river-wetland corridors (e.g., Baker et al., 1993). Although photographs commonly serve as a primary source, they provide little insight into river systems that were modified prior to the advent of photography in the mid-1800s. Maps and written documents provide a longer record. In the United States, records of exploration and General Land Office (GLO) maps made between 1812 and 1946 provide reliable sources of information, especially in the western United States. The GLO surveyed and mapped lands in support of land division and sales to settlers and immigrants. Although the mapping of river corridors was not the intended purpose of GLO maps, river channels commonly served as property boundaries and reference points. Written records accompanied many expeditions and provide a source of supporting information. An example comes from a report submitted to the United States Secretary of War in 1875 describing the valley of the Willamette River, OR, United States, as quoted in Sedell and Froggatt (1984), p. 1830: “[the floodplain] during floods was covered with swiftly-running water to a depth of 1.5–3 m. Each year new channels were opened, old ones closed; new chutes cut, old ones obstructed by masses of drifts; sloughs became the main bed while the latter assumed the characteristics of the former; extensive [wood] rafts are piled up by one freshet only to be displaced by a succeeding one; the formation of islands and bars is in constant progress where the velocity of the current receives a sudden check only to disappear at the very next high water.”

There are, however, significant limitations to using contemporary or historical maps and photographs to determine planform characteristics for small watercourses. Many topographic maps are based on aerial photographs, in which small, well-vegetated streams are typically indiscernible. As a result, stream characteristics such as sinuosity and planform pattern may be missing from historical maps, with small streams represented as simple, straight blue lines that follow the valley centerline. This may give the misleading impression that small streams had, or still have, channels that were straight, single-thread, and static (Beechie et al., 2006; Hall et al., 2007). High-resolution topographic data from Light Detection and Ranging (LiDAR) technology now provides evidence that, prior to anthropogenic disturbance, small watercourses were capable of developing and maintaining river-wetland corridors with multi-threaded planforms (Figure 3).

FIGURE 3

FIGURE 3. Complex, multi-threaded channel planforms can develop in relatively large and small river-wetland corridors: (A) Methow River, Washington, United States; (B) Summit Creek, Oregon, United States.

Historic place names can be more persistent, definitive, and revealing than maps and photographs (Brown et al., 2018). In North America, Native Americans have long used place names related to the presence of river-wetland corridors. Examples include the Entiat River in WA, United States, which means “place of grassy water” in Columbia-Moses, a Southern Interior Salish language; and the Muskegon River, Michigan, derived from the Odawa word “masquigon” for marshy river (Bright, 2004). Early European colonists introduced their own descriptive place names. The term “sausal,” which means “willow” in old, vernacular Spanish, is found in place names in California. GLO maps depict sausals in many California valleys (e.g., Grossinger, 2012) and the place name Sausalito literally means the place with “little willows.” The name of the Embarras River in Illinois has its roots in a French word indicating an “obstacle,” in this case referring to logjams and wood rafts that characterized the river when the French fur-trappers arrived. It is notable that every US state except Hawaii includes at least one Beaver Creek.

In Europe, and particularly in the United Kingdom, “Carr” is a common, ancient place name. It derives from old Norse and means “brushy marsh.” Star Carr in northern Yorkshire, United Kingdom, is an Early Mesolithic archaeological site that was occupied continuously for 200–500 years (Milner et al., 2011). Its valley location, artifacts, and name reveal the pre-historical landscape even though the watercourse is now just a series of highly modified ponds. The United Kingdom place name “Beverley” derives from the Old English words for beaver and lea(h), the latter indicating a “meadow or clearing.”

Current Sparsity

Evidence that river-wetland corridors were wet, widespread, and ecologically productive in the geologic, prehistoric, and recent past is irrefutable. It is well documented that until about two centuries ago, riverine wetlands were still widespread throughout northwestern and central Europe (Grootjans and Verbeek, 2002). However, most of Europe’s lowland rivers had been systematically channelized and their floodplains drained by the end of the 20th century. To understand why, it is necessary only to quote Johann Gottfried Tulla, the purposeful ‘Tamer of the Rhine’, who stated that, “As a rule, no river or stream needs more than one bed, not even the Rhine” (Cioc, 2002, p. 38). With respect to wetlands, between 50 and 90% of wetland ecosystems with organic soils have been lost (Klimkowska et al., 2007), and Krause et al. (2011) estimated that >80% of the remaining floodplain wetlands in northern Germany have been substantially altered since the 1950s.

European colonists carried their propensity for draining valleys and channelizing rivers with them to all corners of the globe. For example, the once-common “chain-of-ponds and meadows” valley floor form largely disappeared from southeastern Australia following European settlement (e.g., Mactaggart et al., 2008). An estimated 90% of New Zealand’s wetlands disappeared within 150 years of the onset of European settlement in 1840 (Ausseil et al., 2007).

Loss of river-wetland corridors is perhaps best documented in the United States. Between the 1780s and the 1980s, six states drained more than 85% of their wetlands and a further 16 drained at least 50% (Dahl and Allord, 1996). In the central prairies, >75% of riverine wetlands along the Platte River have been drained (Riggins et al., 2009) and half of all riparian areas in the arid to semiarid western United States, including their riverine wetlands, have diminished vegetation cover (Silverman et al., 2019). A similarly high degree of riparian disturbance and analogous wetland losses have occurred in montane wet meadows (Loheide et al., 2009).

River-wetland corridors across the United States have also been lost due to channel instability and planform metamorphosis (usually, from multi-thread to single-thread) attributable to a wide variety of anthropogenic actions. Losses may be traced to channelization, dam construction, river regulation, floodplain drainage, artificial levees, restoration to a stabilized single-thread channel, and urbanization (De Becker et al., 1999; Lewis, 2001; Grootjans and Verbeek, 2002). River-wetland corridors may also be degraded by intensive riparian grazing that causes loss of vegetation (Trimble and Mendel, 1995) or extirpation of beaver populations (Wolf et al., 2007; Loheide et al., 2009).

Many of the former river-wetland corridors that remain have been rendered dysfunctional due to dehydration following channel incision that disconnected the stream from its floodplain and drained the hyporheic aquifer (Cluer and Thorne, 2014). Others have been buried under legacy sediment associated with farming (e.g., Happ et al., 1940; Knox, 1987; Booth et al., 2009; Trimble, 2009), mining and logging (Pavlowsky et al., 2017), and other primary industries. Countless river-wetland systems lie buried beneath post-settlement valley fills in the heavily mill-dammed, mid-Atlantic region of the United States (Walter and Merritts, 2008; Merritts et al., 2011; Merritts et al., 2013). In this context, (Walter and Merritts 2008, p. 299) noted that, “… before European settlement, the streams were small anabranching channels within extensive vegetated wetlands.” Only patches of relict Holocene wet meadows remain extant, at locations where dams were not constructed, such as at sparse locations along Gunpowder Falls, Maryland (Merritts et al., 2011) and at Great Marsh, Pennsylvania (Martin, 1958).

Joyce (2014), p. 91 provides a stark assessment of the magnitude of historical loss of wetlands and their ecosystems, “it is likely that the wet grassland resource experienced losses of at least 80% during the 20th century…. In some countries or regions, such as Finland, eastern England, and mid/western United States, it is thought that less than 1% of the former area of wet grassland remains.”

Fundamental Drivers

Somewhat counterintuitively, a functional river-wetland corridor is not predicated by a wet climate, hence these corridors can be found even in an extremely arid zone like that around the River Nile between Khartoum, Sudan and Lake Nassar, Egypt. To understand how this works, consider that, as (Jeffres et al., 2020, p. 7) recently pointed out for California’s Central Valley, “Mean water residence times calculated for the floodplain agricultural wetland, perennial drainage canal and Sacramento River were 2.15 days, 23.5, and 1.7 s, respectively.” It is the longer relative residence time of the water in connected floodplain systems, along with their ability to store groundwater and support riparian vegetation, that give the impression of abundant flow. Thus, a functional river-wetland corridor reflects the presence of a floodplain water table at or near the ground surface throughout most of the year. This high groundwater table and associated abundant surface water can result directly from geologic, biotic, or geomorphic controls, or some combination of these influences (Figure 4). In essence, we view geology, biota, and geomorphology as primary drivers of river-wetland corridors and hydrology as a secondary driver.

FIGURE 4

FIGURE 4. Geologic drivers, biotic drivers, and geomorphic processes and landforms that can promote formation of a river-wetland stream corridor (inset “structure” diagram from usgs.gov).

Geologically, the distinguishing characteristics of a river-wetland corridor are:

(i) a valley floor sufficiently wide to support partially to completely laterally unconfined channel planforms,

(ii) a shallow alluvial aquifer with sufficient capacity and connectivity to keep the river corridor persistently wet, and

(iii) a downstream grade control or valley constriction that acts as the local base level for the upstream reach and modulates longitudinal sediment movement.

The water that hydrates the river-wetland corridor may be predominantly hyporheic (i.e., a component of flow in the river), but may also come from perirheic sources controlled by geology. Geological drivers of upwelling in regional groundwater include grabens that retain groundwater inputs from adjacent uplands (e.g., Koltzer et al., 2019). For example, in the Pantanal of Brazil, Bolivia, and Paraguay, which may be the largest tropical river-wetland corridor, differential subsidence along active faults has created a vast, low-lying sedimentary basin featuring both seasonally and permanently flooded areas (Assine et al., 2015). Similarly, fault scarps in rift valleys can produce drainage systems with wet floodplains that terminate in endorheic lakes like Natron, Eyasi, Manyara, Rukwa, and Balangida in Tanzania (Mwanukuzi, 1993).

Smaller-scale geological drivers of river-wetland formation include:

(i) folding of aquifers (e.g., DesRoches et al., 2014);

(ii) lithologic contacts between units of differing hydraulic conductivity (e.g., Muldoon et al., 2001);

(iii) resistant lithologies that form a local base level and create wet, low-gradient depositional zones upstream (e.g. Klip River, South Africa (Tooth et al., 2002; Tooth and McCarthy, 2007)); and

(iv) undulating bedrock topography that facilitates high water tables where the depth to bedrock decreases locally with distance downstream along the river (e.g., Hardie et al., 2012).

Reach-scale variations in fracture density can also influence valley geometry. Densely fractured bedrock lowers resistance to weathering and erosion, allowing a relatively wide valley floor to form (Ehlen and Wohl, 2002). Dense fractures also support a bedrock aquifer that can generate upwelling of deep groundwater (Briggs and Hare, 2018). Conversely, a relatively shallow impermeable layer or fragipan, such as might be created by lacustrine deposits (e.g., Sudan’s Sudd wetlands along the White Nile upstream of Khartoum (Salama, 1987)) or silica-rich layers, can create a perched aquifer that may be recharged by hyporheic or shallow, perirheic flows (e.g., Bockheim and Hartemink, 2013).

Biologically, the salient features of a functional river-wetland corridor are:

(i) dense riparian and wetland vegetation;

(ii) high organic matter content in floodplain soil; and

(iii) biodiversity.

Aquatic, riparian, and floodplain plants increase drag and surface roughness, resist erosion, and create obstructions to flow both within active channels and across the valley floor (e.g., Collins et al., 2012; Aberle and Järvelä, 2013). In so doing, plants slow surficial flows, augment overbank flows, and promote the influent stream conditions that help to hydrate a river-wetland corridor. Other biotic features documented as being capable of driving hyporheic exchange and influent stream conditions include: beaver dams (Polvi and Wohl, 2012); large wood, especially in the form of logjams or wood rafts (e.g., Triska, 1984; Miller et al., 2012; Larsen et al., 2016); and dense stands of aquatic, herbaceous, and/or shrubby vegetation (Larsen and Harvey, 2011; Larsen, 2019). The capacity of woody and shrubby vegetation to “clog” streams has long been recognized—hence the penchant of drainage authorities for channel maintenance that involves “clearing and snagging” (Shields and Nunnally, 1984; Harmon et al., 1986; Gippel, 1995). However, in low gradient fluvial systems like the Florida Everglades (Larsen and Harvey, 2010) and many mountain meadows, dense covers of native grasses create sufficient resistance to flow and erosion to mediate channel form and migration, promote sediment retention, and support a diverse and dynamically stable river-wetland corridor (Micheli and Kirchner, 2002a; Micheli and Kirchner, 2002b; Slocombe and Davis, 2014).

High organic matter content in floodplain soils can increase soil cohesion (Zhang and Hartge, 1990) and tensile strength (Rahimi et al., 2000) and thus resistance to erosion. High organic matter content can also increase porosity and permeability and therefore surface-subsurface hydrologic connectivity.

Biodiversity refers to the diversity of organisms that can influence river processes, from biofilms and macroinvertebrates that help to stabilize fine sediment (Albertson et al., 2019; Gerbersdorf et al., 2020), through crustaceans (Johnson et al., 2011) and fish (Hassan et al., 2008) that alter the grain-size distribution and cohesion of streambed sediments, to apex predators that limit grazing intensity in the river corridor and therefore influence the vegetation communities and food and habitat for other animals such as beaver that are dependent on riparian vegetation (Beschta and Ripple, 2012).

Geomorphic processes and landforms can promote formation of river-wetland corridors and they commonly generate within-reach variability by creating local or temporary base levels and/or valley width constrictions. Landforms that may constrict the valley floor include:

(i) alluvial tributary fans (e.g., Miller et al., 2012) and

(ii) run-out deposits, fans, and lobes generated by valley side slope failures such as

a. rock falls (Schrott et al., 2003),

b. rock avalanches,

c. landslides,

d. solifluction lobes, and

e. debris flows (Swanger et al., 2010; Booth et al., 2020).

A geomorphically-generated valley floor constriction must be relatively large and enduring in order to impede flow and sediment transport in the trunk stream sufficiently to create an upstream depositional reach with a high water table (Fryirs et al., 2007). Elevated sediment inputs from tributaries and valley side slopes that can create such relatively large landforms may be triggered by particular disturbances such as volcanic eruptions (e.g., Del Moral, 1999) or wildfires (e.g., Heede et al., 1988; Benda et al., 2003). Excessive and protracted sediment inputs from the catchment and trunk stream upstream can also cause so much downstream valley alluviation that surficial runoff switches from single-channeled to multi-threaded or even sheet flow spread across the valley floor - a scenario that can persist for decades in river corridors where high sediment loads prevail (e.g., Fryirs et al., 2007; Martin-Vide et al., 2014; Major et al., 2019).

Figure 5 relates planform variation to the influence of geomorphic landforms, which generate local variability in valley floor width, hydrologic connectivity, and partitioning of water between surface and subsurface flows within a single, contiguous river-wetland corridor. The expression of diverse planforms in this example is dynamic in time as well as space, changing in response to fluctuations in discharge, sediment flux (fluvial and upland inputs), vegetation growth and dieback, and the actions of animals ranging in size from algae and macroinvertebrates to large herbivores and beaver (Johnson et al., 2019). The hyporheic segment of river flow is in very close proximity to the valley-floor surface and at base flow supports a mosaic of features with and without surface hydrologic connectivity. This river-wetland corridor includes valley-spanning wetland complexes, a single-thread channel, a segment with no channel, spring brook heads, and anabranching channels.

FIGURE 5

FIGURE 5. Example of variability in channel planform and partitioning of water between channels, wetlands, and the shallow aquifer within a single, contiguous river-wetland corridor. Large tributary fans on the northern boundary are easily discernible, while smaller fans on the southern boundary have been highlighted to show their influence on fluvial processes within this continuous valley. North Fork Crooked River, Oregon, United States.

Glacial moraines that act as a local base level and temporarily dam a stream can create a depositional zone upstream from the moraine (Cooper et al., 2012) and glacio-fluvial deposits in valley sandurs and outwash plains usually have a high water table (e.g., Scheffel, 2018; Perera, 2020), making them potential reaches for river-wetland corridor formation. Alpine glaciers also tend to create a stepped valley floor topography, with low-gradient and steeper segments of valley floor alternating downstream (MacGregor et al., 2000). The low-gradient valley segments may support river-wetland corridors (e.g., Arp et al., 2007).

Interactions and Feedbacks

Although it was convenient to introduce and describe the attributes, drivers, processes, and landforms associated with river-wetland corridors separately, it is their interactions that govern hydrologic connectivity, channel form and evolution, and vegetation dynamics. Continuous changes in the relative influences of the drivers and processes, coupled with the complexity of nested feedback loops between river-wetland corridor morphologies and ecosystems, make these systems both responsive to change and resilient to natural disturbance. Nevertheless, river-wetland corridors are vulnerable to the impacts of anthropogenic activities. We first describe the interactions that occur in natural systems and then discuss how a wide array of human activities alter these interactions.

In a pristine river-wetland corridor, geology and geomorphic processes interact to create a characteristic valley geometry with a relatively wide valley floor and gentle downstream valley gradient. Geology, biotic communities, and geomorphic processes then interact to create degrees of lateral and vertical connectivity that are similar in magnitude to that of longitudinal connectivity. These same fundamental drivers also govern the inputs of water, sediment, and organic matter to the river corridor and, in turn, these inputs interact with the valley characteristics to influence river form and process (Figure 6).

FIGURE 6

FIGURE 6. Schematic representation of a fully connected stream corridor where biogeomorphic processes (e.g. large wood, beaver, vegetation) and river-wetland attributes (e.g. valley geometry, channel planforms, channel migration, hyporheic and regional aquifers) interact in complex ways, via multiple, nested feedback loops. Original illustration provided by LandStudies, Inc., Pennsylvania (with permission from Land Studies, 2021).

Channel form, conveyance capacity, and boundary conditions then interact with water, sediment, and organic inputs to influence rates and distributions of lateral channel migration. However, the relationship between processes driving and resisting lateral migration is complicated by two, competing feedback loops. In the first feedback loop, lateral migration influences the distribution, density, and erosional resistance of floodplain vegetation by determining the turnover time and spatial heterogeneity of valley-floor surfaces (e.g., Fetherston et al., 1995; Beechie et al., 2006). In the second feedback loop, vegetation moderates the influence of lateral migration by increasing hydraulic roughness and reinforcing floodplain soils, which act to increase the erosional resistance of channel banks, while also facilitating deposition of coarser sediments that form natural levees and fine, cohesive sediments that resist re-entrainment (e.g., Micheli and Kirchner, 2002a; Allen et al., 2018).

Vegetation type and density, which reflect the regional climate, biome, and depth to alluvial aquifer, also influence the amount and spatial distribution of large wood in the stream corridor (e.g., Wohl et al., 2017b) and, in the northern hemisphere, the presence of beaver (Castor canadensis in North America, C. fiber in Eurasia) (Pollock et al., 2017). Obstructions within the active channel(s) and floodplain associated with the presence of vegetation, large wood, and beaver dams increase subsurface hydrologic connectivity and hyporheic exchange flows (e.g., Sawyer and Cardenas, 2012; Wang et al., 2018; Doughty et al., 2020). Similarly, these obstructions can further influence surface hydrologic connectivity by promoting lateral channel migration (e.g., Eaton and Hassan, 2013), formation of a multi-threaded channel planform (John and Klein, 2004; Collins et al., 2012; Polvi and Wohl, 2013), and enhanced overbank flows (Brummer et al., 2006; Westbrook et al., 2006). Local variability in hydrologic connectivity, in turn, influences the elevation of the floodplain water table, which directly affects the types, densities, and vitality of vegetation. This reflects an additional, strongly positive feedback between enhanced hydrologic connectivity and biologic processes.

Stratigraphic and geochronological studies of river-wetland corridors indicate that feedbacks among water, sediment, and biota can create and maintain a dynamically stable alluvial valley floor that may endure for centuries to millennia (e.g., Gibling et al., 1998; Polvi and Wohl, 2012). This is evidence that a fully functioning river-wetland corridor is not a transient state but a dynamically stable river type that is naturally resilient to all but major, step-change disturbances (such as tectonic uplift or sea level decline).

This resilience to disturbance stems from the bio-geomorphological complexity and nested feedback loops that create and maintain river-wetland corridors. Hey (1978) proposed that a single channel has nine degrees of freedom in adjusting its morphology to accommodate changes in boundary conditions and inputs. In a multi-threaded river-wetland corridor the number of degrees of freedom increases linearly with the number of channels and the number of possible combinations of ways of accommodating disturbance grows rapidly to hundreds of thousands or even millions (see Supplementary Material). Leopold (1994) demonstrated that river responses to disturbance are distributed among all available degrees of freedom. In essence, when subject to an external perturbation, a river-wetland corridor can diffuse the impact of that disturbance through thousands of small adjustments that are distributed throughout the complex river corridor. This helps explain why a river-wetland corridor is capable of absorbing substantial disturbances while staying within the bounds of its dynamic stability.

In a fully functional river-wetland corridor, this intrinsic, geomorphic resilience to disturbance is further enhanced by riverine biota. Beaver modifications of the river corridor increase resilience to drought (Hood and Bayley, 2008) and wildfire (Fairfax and Whittle, 2020). The dense vegetation of river-wetland corridors can enhance the resistance of these systems to flood-induced erosion and deposition (Heffernan, 2008). Dense wetland vegetation can also create a condition of dynamic stability in which changes in hydrology drive shifts in the areas of emergent vegetation versus open water (Larsen and Harvey, 2010). Additionally, and significantly, the recuperative capacity of vibrant river-wetland ecosystems gives the system a capacity to “self-repair” that simpler, water- and sediment-dominated streams do not exhibit to the same degree. This not only hastens post-disturbance recovery and shortens relaxation times, but can also increase ecosystem resilience to future disturbances (Johnson et al., 2019).

The dynamically stable and resilient nature of river-wetland corridors stems from their capacity for continuous, small adjustments that accommodate fluctuations in the influences of hydrology, geology, and biota on river form and process (Castro and Thorne, 2019). Externally driven, episodic changes such as major floods, volcanic eruptions, or wildfires significantly disturb the intricate balance between water, sediment, and biota (Kleindl et al., 2015), but the path by which the biogeomorphic system has evolved triggers systemic interactions that diffuse, mitigate, and ultimately absorb all but the most profound and persistent shocks. For example, when successive generations of beavers shift the locations of dams and ponds across a river corridor over periods of decades to centuries, they create a spatially heterogeneous river corridor (Laurel and Wohl, 2019). Many investigators have described the characteristics and importance of spatial heterogeneity in river-floodplain systems (Wohl, 2016), leading to descriptions such as “shifting habitat mosaics” (Arscott et al., 2002; Stanford et al., 2005). In a river-wetland corridor, the details of the riverscape change daily, giving it greater fluidity even than a shifting mosaic. We therefore propose the term “kaleidoscope river” to describe the self-organizing tessellation of the polydimensional river-wetland corridor, a system continually adjusting to internal and external perturbations in ways that collectively maintain configurations that are robust and self-reinforcing. A kaleidoscope is essentially a continually changing mosaic, so using the word kaleidoscope in this context emphasizes the continually dynamic nature of river-wetland corridors.

Anthropogenic Modifications and Contemporary Remnants

Despite their natural resilience, river-wetland corridors can be destabilized by diverse forms of human-induced disturbance. River-wetland corridors worldwide have been and still are commonly altered for flood control, navigation, hydropower generation, downstream transport of commodities such as cut logs, and to open access to agriculturally rich bottomlands through land drainage (e.g., Schrautzer et al., 1996; Schneider and Eugster, 2007). Channel modification routinely involves channelization (e.g., Brookes, 1988; Pisut, 2002; Mitsch and Day, 2006; Brown et al., 2018) and removal of naturally occurring wood rafts, logjams, and individual wood pieces (e.g., Harmon et al., 1986; Wohl, 2014). The almost complete eradication of beaver populations for the commercial fur trade (e.g., Nolet and Rosell, 1998; Pollock et al., 2017) also caused widespread hydrologic disconnection and simplification of river-wetland corridors. In the United States, national programs such as the Swamp Land Act of 1850 transferred title of federally owned wetlands to states that would agree to drain the land and convert it to agricultural uses. This federal legislation hastened the destruction of millions of hectares of wetlands (e.g., 8.1 million ha in Florida, 3.5 million ha in Louisiana) (Guirard and Brassieur, 2007). Analogously, landscape drainage overseen by Dutch engineers resulted in widespread degradation of the English Fens during the middle decades of the 17th century (Williamson, 2006).

Even if riverscapes are not altered directly, changes in land use and water management can result in significant changes to flow regimes, sediment loads, valley floor and channel geometries, water surface slopes, and riparian biota. This is evidenced particularly by human impacts on catchment inputs to drainage networks and the degrees to which water, sediment, and wood moving through the river corridor are exchanged between the channel, floodplain, and hyporheic zones of the river.

In this context, it is difficult to overstate the significance of the complex, nested feedback loops outlined above, within which a change in any of the driving variables can be accommodated through myriad, subtle changes in the configuration and dynamics of the river-wetland corridor, while maintaining continuity of the river functions. Removing or converting vegetation, large wood accumulations or beaver dams, for example, can reduce lateral surface and subsurface hydrologic connectivity, reduce channel migration rates, and prompt a multi-threaded system with low-conveyance and limited downstream connectivity to metamorphose into a single-thread, high-conveyance channel (Collins et al., 2002; Wolf et al., 2007). Similarly, removal of logjams, beaver dams, and other temporary, local base level controls can trigger channel incision and lowering of the floodplain water table, which drains floodplain aquifers and wetlands (e.g., Larsen et al., 2016) and converts riparian vegetation to upland species. Removal of apex predators can result in unnaturally intensive riparian grazing by large ungulates, leading to loss of vegetation and beaver that can result in desiccation of the river-wetland corridor and channel incision (e.g., Beschta and Ripple, 2006; Beschta and Ripple, 2012).

Construction of levees or embanked roads artificially reduces valley floor width, which may transform a multi-thread planform to a single-thread, high-conveyance channel. Reduced flood flows and sediment supply in regulated rivers can also decrease channel migration rates (e.g., Bradley and Smith, 1984), limit surface and subsurface hydrologic connectivity (e.g., Kingsford, 2000), lower the floodplain water table (Mahoney and Rood, 1991), and allow xeric, upland vegetation to encroach into the floodplain (e.g., Caskey et al., 2015). In other circumstances, increased base flows and reduced flood peaks can allow floodplain vegetation to increase bank erosional resistance, raise the floodplain water table, and cause a braided river to assume a meandering or anastomosing planform (e.g., Williams, 1978; Nadler and Schumm, 1981).

Less direct, but perhaps no less consequential impacts to river-wetland corridors may stem from landscape-scale changes in vegetation beyond the valley floor. Benda et al. (2003), for example, concluded that timber harvest and fire suppression can substantially alter the frequency and magnitude of natural disturbances, such as fire-induced mass movements that create or enlarge the alluvial fans that sustain some river-wetland corridors. These types of effects are pervasive across large, relatively dry and fire-prone areas of the world, such as the Mediterranean region and the western United States (Shakesby and Doerr, 2006).

Despite extensive modification and loss of river-wetland corridors, examples of this type of riverine environment can still be found. Typically, functional river-wetland corridors remain in mountainous or high-latitude areas of the world that are too cold for farming; in exceptionally wet areas where either the land could not be effectively drained or salinization destroyed soil fertility; and in extremely large river systems where channelization was not economically feasible (e.g., portions of the Amazon and Congo River basins; Keddy et al., 2009).

Contemporary examples can be found in locations ranging from the few remaining relatively natural river deltas, such as those of the Yukon, Mackenzie, and Lena Rivers, through estuarine floodplains and tidal marshes (e.g., Salmon River, OR, United States), to headwater streams and wet meadows. Many of these, however, are relatively small remnants of formerly more longitudinally and laterally extensive river-wetland corridors, Larger, intact river-wetland corridors also remain in parts of Africa, Central Asia, Siberia, and South America. Table 1 and Figure 1 highlight a few, diverse examples of these remnants.

TABLE 1

TABLE 1. Contemporary examples of remaining river-wetland corridors.

Significance

The significance of river-wetland corridors as a river type extends from local scales to cumulative effects at regional and global scales. This significance stems from the diverse river functions that river-wetland corridors provide (Figure 7). Major river functions can be grouped into conveyance, storage and processing, habitat and biodiversity, and resilience.

FIGURE 7

FIGURE 7. Schematic illustration of river functions associated with river-wetland corridors (“biodiversity” image modified from Nelson et al. (2006); “denitrification” diagram from ibiologia.com; “food supply” image (rotifers) from Matthew A. Robinson, Wikimedia Commons).

The primary function of a river is to convey water, sediments, and organic materials from upstream sources to downstream sinks. In this context, based on the arguments and explanations set out in previous sections, river-wetland corridors play an important role in modulating downstream connectivity and locally promoting enhanced lateral and vertical connectivity. Studies of contemporary rivers with valley segments occupied by remnant river-wetland corridors indicate the important contributions of this river type to the geomorphic and ecological functionality of a river system (Poff et al., 2007; Peipoch et al., 2015).

Intact river-wetland corridors attenuate downstream fluxes of water, solutes, sediment, and particulate organic matter (POM) and, in so doing, enhance organic carbon storage (e.g., Robertson et al., 1999; Johnston, 2014; Sutfin et al., 2016; Laurel and Wohl, 2019; Sutfin and Wohl, 2019) and denitrification (e.g., Richardson et al., 2004; Racchetti et al., 2010). The temporally limited longitudinal connectivity that river-wetland corridors impart to the fluvial system can be beneficial, especially when accompanied by enhanced lateral and vertical connectivity (Battin et al., 2008; Burchsted et al., 2010; Wohl, 2017). Increased lateral and vertical connectivity amplifies the capacity of river-wetland corridors to store sediment and adsorbed contaminants, and the saturated, reducing environment and high primary productivity typical of a river-wetland corridor (Edwards et al., 2020) can support high concentrations of soil organic carbon (e.g., Keddy et al., 2009; Sutfin et al., 2016; Lininger et al., 2018). Field quantification of river corridor carbon storage establishes that the reaches in a stream network with well-connected, wet floodplains can have disproportionately high soil organic carbon stock compared to other, drier valley-floor segments (Wohl et al., 2012; Wohl et al., 2017a; Sutfin and Wohl, 2019). They can also be disproportionately important at the catchment-scale in terms of storing far more organic carbon per unit area than adjacent uplands (Wohl et al., 2012), suggesting that river-wetland corridors could, and probably should, be effectively targeted for restoration intended to enhance carbon sequestration (Wohl et al., 2018).

Hydraulic complexity and the abundance of low-velocity areas within a river-wetland corridor can facilitate retention of POM (e.g., Jones and Smock, 1991), especially where extensive backwater areas are created by logjams (Beckman and Wohl, 2014; Livers et al., 2018) or beaver dams (e.g., Naiman et al., 1986). In turn, POM retention increases the capacity of these systems to support fish and wildlife because food availability is a first-order control on biological populations (Lindeman, 1942; Odum et al., 2005).

Some river-wetland corridors are predominantly forested and these shaded systems rely on POM shed by floodplain forests as an energy source (e.g., Mulholland, 1981; Thompson and Townsend, 2005). Rivers in wet meadows are less shaded than those in forests, so that instream photosynthesis by algae, bryophytes, and aquatic macrophytes, along with the presence of decaying floodplain vegetation, provide the base for the aquatic food web (e.g., Thorp et al., 1998). Retention of POM remains important, however, both as a food source and as habitat for microbial and macroinvertebrate communities (Tank et al., 2010; Edwards et al., 2020).

By facilitating in-channel and, especially, overbank storage of fine sediment and adsorbed contaminants such as heavy metals, synthetic chemicals (Wohl, 2015), and excess phosphorus (Reddy et al., 1999), river-wetland corridors also provide opportunities for microbial communities that promote denitrification to access more slowly moving surface and subsurface waters, which helps to improve water quality. High rates of hyporheic exchange in river-wetland corridors can also dampen seasonal and daily temperature fluctuations in surface waters (e.g., Loheide and Gorelick, 2006; Weber et al., 2017) in a manner beneficial to fish and other aquatic organisms.

Functional river-wetland corridors provide both abundant and diverse aquatic and riparian habitat (e.g., Sayer, 2014; Entwistle et al., 2019) and corridors for species migration and dispersal (e.g., Antas, 1994). The spatial and temporal sequence of disturbances associated with processes such as lateral channel movement, formation of logjams (Collins et al., 2012), and construction and then infilling of beaver ponds (Wright et al., 2002; Stevens et al., 2006) creates a patchy, shifting pattern of surface and subsurface habitats. These habitats have diverse grain-size distribution, elevation, hydraulic conductivity, hydrologic connectivity, inundation regimes, organic carbon concentrations, and nutrient availability. Because of this diversity, floodplain wetlands are a rich source of food for juvenile salmonids (Katz et al., 2017), which can be acquired directly by the fish accessing the floodplain or can be delivered to the channel network by floodplain return flows (Jeffres et al., 2020).

Wetlands and beaver ponds of varying age and size support juvenile salmonids, but also create critical habitat diversity for wetland plants, amphibians, and other species that require a reliable water source (Stevens et al., 2006; Popescu and Gibbs, 2009). This increased “density diversity” enhances the opportunity for aquatic species to find the appropriate life-history habitat within a relatively small area, effectively reducing migration distances and energy expenditure. The hydraulic and habitat heterogeneity associated with functioning river-wetland corridors decreases the distances between various habitat niches so that aquatic and wetland species do not need to move as far to fulfill diverse thermal and trophic needs (Armstrong and Schindler, 2013). Spatial variations in flow depth and velocity also allow aquatic and wetland species to self-segregate. For example, juvenile salmonids can find refuge in shallow water areas away from piscivorous fish (Brown and Moyle 1991), while different species of pond-breeding amphibians have higher survival rates where beaver ponds of differing age and hydrologic connectivity provide habitats with and without fish (Cunningham et al., 2007).

The river functions described above result in expansive areas with higher densities of biomass and higher biodiversity within river-wetland corridors than may be present in more laterally confined portions of a stream network (e.g., Thorp et al., 2010; Bellmore and Baxter, 2014; Shi et al., 2017). Beaver-modified valley floors, for example, have higher biodiversity of aquatic and wetland plants (Wright et al., 2002), aquatic and terrestrial insects (e.g., Hood and Larson, 2014), amphibians (e.g., Karraker and Gibbs, 2009), fish (e.g., Smith and Mather, 2013), birds (e.g., Aznar and Desrochers, 2008), and mammals (Rosell et al., 2005; Hauer et al., 2016). Greater biodiversity, coupled with the higher levels of habitat complexity and diversity described previously, may increase the stability of biological populations subject to significant environmental variability (Bellmore et al., 2015). This in turn increases the range, value, and reliability of a suite of ecosystem services highly valued by society (Ekka et al., 2020).

An important, tertiary river function provided by river-wetland corridors is that of enhancing the resistance and resilience of the river corridor to both natural and human disturbances. Resistance describes the ability of a system to remain essentially unchanged when subject to disturbance (e.g., Simon, 2009). Resilience is the persistence of relationships within a system and is a measure of the ability of the system to absorb changes of state and driving variables (Holling, 1973). River-wetland corridors are generally more resistant to drought and wildfire because of the elevated water table and relative abundance of standing water (e.g., Hood and Bayley, 2008; Fairfax and Whittle, 2020). Sediment pulses that can severely damage dysfunctional channels in the aftermath of wildfire are instead distributed and attenuated across functional river-wetland corridors, resulting in less significant impacts. River-wetland corridors can also be more resistant to floods because wide, vegetation-stabilized floodplains and, in some cases, the presence of multiple channels, attenuate flood peaks and reduce hydraulic force per unit area exerted against the channel and floodplain boundaries (e.g., Hillman, 1998; Nilsson et al., 2018). Related to these characteristics, river-wetland corridors are particularly suited to subsurface water storage (e.g., Loheide and Gorelick, 2007), a river function that may help to support or enhance local and downstream base flows (Wegener et al., 2017).

Implications for River Restoration

River restoration, as commonly practiced today, reflects an aesthetic preference for a well-defined single channel that is relatively stable (Kondolf, 2006; Le Lay et al., 2013; Medel et al., 2020; Wilson et al., 2020), with channel conveyance that limits the frequency and duration of floodplain inundation. This results in restored rivers with channel geometries, planforms, and capacities for conveying water, sediment, and organic matter that mimic those characteristic of transport reaches (i.e., reaches that pass excess sediment downstream; Montgomery and Buffington, 1997). Channels with these characteristics are suitable restoration targets for valley segments with relatively narrow valley floors and floodplains, relatively high channel gradients, strong downstream connectivity, and limited capacity for surface or subsurface storage (Jeffres et al., 2020). However, mimicking transport channels is less suited to wider, lower-gradient, depositional valley reaches that, prior to anthropogenic disturbance, featured the multi-threaded, response channels (i.e., reaches that were likely to accumulate excess sediment; Montgomery and Buffington, 1997) that are characteristic of river-wetland corridors.

Maintenance or restoration of a high-conveyance, transport channel where there would naturally be a response channel limits lateral and vertical connectivity within the river corridor, missing the opportunity to re-create the functions of the lost river-wetland corridor and perpetuating the conditions within which a defined single-thread channel is bounded by a relatively dry, former floodplain. What could be above- and below-ground storage areas for water, sediment, organic matter, and nutrients remain sources as the valley floor continues to be functionally disconnected and efficiently drained. This inhibits recovery of the complex interactions and feedback loops between biogeomorphic processes and river-wetland attributes described above and illustrated in Figures 4 and 7, as well as degrading the habitat networks provided by hydrologically connected and dynamically stable channels and floodplain wetlands (Sayer, 2014). In essence, replacing a dynamically stable river-wetland corridor with a more static channel that is largely disconnected from the floodplain changes a kaleidoscope river to the fluvial equivalent of a monochromatic photograph.

In the past, most river networks included response reaches featuring river-wetland corridors that were interspersed with source and transport reaches. Response reaches are known to provide a range of intrinsically valuable river functions. This suggests that river management and restoration should recognize the former abundance of this river type in diverse landscape settings. Management and restoration should include river-wetland corridors in conceptualizations of desirable river types and should, where appropriate and feasible, consider river-wetland corridors as potential, alternative targets for river conservation and restoration projects. Given the multi-faceted significance of river-wetland corridors, investing in their re-creation can represent a wise use of the limited funds available to support river restoration.

Restoration explicitly designed to restore river-wetland corridors is gradually starting to occur, as exemplified by wet-meadow restoration in Europe (Grootjans and Verbeek, 2002; Klimkowska et al., 2007) and the United States (Booth et al., 2009; Riggins et al., 2009; Hartranft et al., 2011; Silverman et al., 2019; Voosen, 2020), “stage 0” restoration projects in the United States Pacific Northwest (Powers et al., 2019), and beaver reintroduction and mimicry efforts throughout the United States (Pollock et al., 2014; Bouwes et al., 2016; Pollock et al., 2017), Canada (Muni and Westbrook, 2021), Europe (e.g., Nolet and Rosell, 1998; Fustec et al., 2001), and across the United Kingdom (Puttock et al., 2015). To be successful, restoration requires a sound understanding of past and present conditions and trajectories, informed by analyses of historical records and key biogeomorphic processes across a range of spatial and temporal scales (e.g., Woelfle-Erskine et al., 2012; Rathburn et al., 2013; Brierley and Fryirs, 2016). Many existing restoration efforts focus on small to medium-sized rivers. Although large floodplain rivers have already been extensively modified in the temperate latitudes and are threatened by projected human alterations in both tropical and high latitudes (e.g., Erӧs et al., 2019), these rivers can be more difficult to restore because of the presence of multiple land owners and jurisdictions, as well as numerous constraints created by infrastructure and consumptive water uses. Nevertheless, larger scale manipulations of river-corridor topography and flow regime designed to restore the hydrologic connectivity that supports river-wetland corridors can be undertaken to beneficial effect, as in the case of the Kissimmee River in Florida, United States (Koebel and Bousquin, 2014).

In closing, we stress that not every reach in a river network is a candidate for river-wetland corridor restoration, or even river-floodplain reconnection. However, in order for impaired systems to fulfill their potential to deliver multiple functions and benefits, at least some of the wider, flatter, alluvial valley segments that punctuate source and transport reaches should feature river-wetland corridors. This is achievable if restoration practitioners and regulators embrace two paradigm shifts. The first hinges on acknowledging the past abundance of river-wetland corridors and appreciating their potential to contribute to the functionality and resilience of river systems in what is an uncertain future. The second rests on broadening our view of the river, by thinking outside the channel.

Author Contributions

All of the authors contributed to writing the text and compiling the information in the table by adding relevant information, examples, and references; JC, EW, and PP are primarily responsible for the figures with the exception of Figure 6, which is used courtesy of LandStudies.

Funding

In part, this work was supported by the Engineering and Physical Sciences Research Council, United Kingdom (grant number EP/P004180/1).

Disclaimer

The findings and conclusions in this manuscript are those of the authors and do not necessarily represent the views of NOAA-Fisheries, the US Fish and Wildlife Service, or the US Forest Service.

Conflict of Interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Acknowledgments

We would like to thank Ryan Bellmore for his insights on the capacity of ecosystems to support fish and how habitat complexity and diversity confer stability to biological populations. We also would like to thank special issue editors Fernando Nardi, Ryan Morrison, Paola Passalacqua, and Ryan McManamay for the invitation to contribute this paper. We thank Lyle Zevenbergen for preparing the spreadsheet on river degrees of freedom that is included in the Supplemental Material.

Supplementary Material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2021.653623/full#supplementary-material

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