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River Restoration and Climate Change: Some ReflectionsMatt KondolfUniversity of California Berkeley
NBWA, Petaluma, April 2008
We can consider both-How climate change will affect our efforts to restore rivers-How river restoration could be used to mitigate effects of climate change
Consider our favorite charismatic megafauna, anadromous Pacific salmon
First: Northern California will become more like southern Calif: more episodic
Uvas Creek, California Jan 1996, 2 mo post-construction (Are we in Denmark?)
This means our attempts to mimic humid climate forms, such asundertaken on Uvas Ck in Gilroy, are even less likely to succeedthan they have to date
Uvas Ck (same view as last photo) July 1997 Channel failed Feb 1996, 3 months after construction
Design for the Climate/hydrologyCultural preference for single-thread meandering channels – like green lawns – probably inherited from Atlantic climates -18th-19thC English landscape theory, more recent research
Anticipating higher Temps: Using Butte Creek spring run to re-populate a restored San Joaquin
Deer Creek
Using river restoration to (partially) mitigate effects of climate change: Deer Creek
Restoration planning documents for salmon in the Sacramento River system identified the need for smaller gravels and more riparian trees in Lower Deer Ck. Recommended: add spawning gravel, plant trees
But a geomorphic analysisshowed that the conditions of large gravel and lack ofvegetation along low-flowchannel were consequencesof a 1949 flood control project
Pre-1949 channel: multi-threaded, complex, shaded, frequent pool-riffle alternations, hydraulically rough
Post-1949 channel: simplified, wider, hydraulically smooth
High shear stress in floods, gravels and trees would scour
Confinement by levees increases bed shear stress during high flows
Deer Ck Strategy:
Allow overbank flow to relieve excess shear stress in channelNo channel maintenance
Because watershed is largely unaltered, flow and sediment load should lead to re-establishing channel complexity
Complex channel induces more hyporheic exchange, buffering water temperatures
Tail of R
iffle
Head of R
iffle
Middle of R
un
Head of R
iffle PoolH
ead of Riffle
Head of C
huteH
ead of Riffle
Head of R
unH
ead of Riffle
Head R
iffleH
ead of Run
Head of R
iffleH
ead of PoolH
ead of Riffle
Head of R
un
Head of R
iffleH
ead of Run
Head of R
iffleH
ead of Run
Head of R
iffle
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un
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iffle
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un
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iffle
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unT
ail of Riffle
Head of R
iffle
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Station (feet upstream of Sacramento River Confluence)
Ele
vati
on (
ft)
Flow
Figure 3.2‑2: Longitudinal profile of thalweg in a geomorphically complex reach of lower Deer Creek near RM 9.
Head of R
iffle
Head of R
iffle
Top of B
eaver Dam
Beaver D
am P
ool
Run U
S of Beaver D
am
Head of P
ool
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Station (feet upstream of Sacramento River Confluence)
Ele
vati
on (
ft)
Flow
Figure 3.2‑1: Longitudinal profile of thalweg in a geomorphically simple reach of lower Deer near RM 1.
Q
main channel (low elevation)Qside channel (high elevation)
Q
downwelling “source” water
upwelling hyporheic water
cobble bar or island
Figure 3.3‑6: Schematic of typical hyporheic exchange temperature study site in lower Deer Creek.
Figure 3.3‑5: Upwelling hyporheic water identified by tracer dye test.
Downwelling source water “pod”
Upwelling hyporheic water piezometers
Figure 3.3‑7: Picture of typical hyporheic exchange study site in lower Deer Creek near RM 5.0. Flow direction is from top to bottom of picture.
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ary-
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y-05
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ch-0
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ust-
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ber-
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w (
cfs
)
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mp
erat
ure
(°C
)
Flow at USGS Gage (cfs) Flow at SVID (cfs) Temperature (°C)
Figure 3.4‑4: Comparison of mean daily streamflow at USGS gage (approximately RM 10.5), streamflow downstream of the SVID dam (approximately RM 2.4), and water temperature at the USGS gage.
Figure 3.3‑9: Typical downwelling (left) and upwelling (right) temperature sensor installations in lower Deer Creek.
Downwelling Peak
Upwelling Peak
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0 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24
Time (hours)
Tem
pera
ture
(°C
)
Downwelling Water Upwelling Water
Upwelling Amplitude
Downwelling Amplitude
LagTime
BetweenPeaks
Peak Reduction
Figure 3.4‑10: Illustration of peak water temperature reduction, water temperature amplitude fluctuation reduction, and lag time between peaks measured at downwelling and upwelling hyporheic exchange sites. Data from hyporheic exchange site at RM 5.0 for August 1, 2005.
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Time (days)
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pera
ture
(°C
)
Downwelling Water Temperature (°C) Upwelling Water Temperature (°C)
Figure 3.4‑16: Hyporheic exchange sensors near RM 5.0 for a 6 day period in August, 2005.
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Time (days)
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per
atu
re (
°C)
Downwelling Water Temperature (°C) Upwelling Water Temperature (°C)
Figure 3.4‑22: Hyporheic exchange sensors near RM 6.9 for a 6 day period in August, 2005.
Salmonid juvenile at upwelling site in July when surrounding water temps reach 30+ C!
Often: irrevocable changes to the system, restoration of only some functions possible
Viewing directions of anthropic change/restorationin terms of connectivity and flow variability
We see restoration trajectories rarely parallel degradation trajectories
Streamflow variabilitylow high
Long
itudi
nal c
onne
ctiv
itylo
whi
gh
spring fed snowmelt rainfall ephemeral/intermittent
DeschutesRiver, Oregon
Butte Ck California
Isar River, Germany
Crow Creek, Tennessee
Torrens River,South Australia
Condamine-Balanne, Queensland
flow
reg
ulat
ion
(dam
)
perennialization by urbanization,
weirs, and wastewater
channelization
off-stream storages
divert base flow
rehabilitation
rehabilitation
reha
bilit
atio
n
Clear Creek, California
flow
regu
latio
n (d
am)
Kondolf et al. in review
The road ahead for river restoration:
Let’s avoid building SUVs!