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| [[File:PDO Pattern.png|thumb|300px|PDO positive phase global pattern]]
| | 41 year-old Telecommunications System Planner Billy from Trail, enjoys blogging, diet and crochet. Recently has visited Mudejar Architecture of Aragon.<br><br>Feel free to surf to my web blog - [http://simpledietburnfat.com/simple-diet-diet-plan-to-burn-foods-that-burn-fat-and/ how to lose weight fast] |
| The '''Pacific Decadal Oscillation''' (PDO) is the leading [[Empirical orthogonal functions|EOF]] of monthly [[sea surface temperature]] anomalies (SSTA) over the North Pacific (poleward of 20° N) after the global mean SSTA has been removed, the PDO index is the standardized [[principal component]] time series.<ref>{{cite journal|last=Deser|first=Clara|coauthors=Alexander, Michael A.; Xie, Shang-Ping; Phillips, Adam S.|title=Sea Surface Temperature Variability: Patterns and Mechanisms|journal=Annual Review of Marine Science|date=January 2010|volume=2|issue=1|pages=115–143|doi=10.1146/annurev-marine-120408-151453}}</ref>
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| The PDO is detected as warm or cool surface waters in the [[Pacific Ocean]], north of 20° N. During a "[[Ocean heat content|warm]]", or "positive", phase, the west Pacific becomes cool and part of the eastern ocean warms; during a "cool" or "negative" phase, the opposite pattern occurs. It shifts phases on at least inter-decadal time scale, usually about 20 to 30 years.
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| The Pacific (inter-)decadal oscillation was named by Steven R. Hare, who noticed it while studying [[salmon]] production pattern results in 1997.<ref name="Mantua1997">{{cite journal |last=Mantua |first=Nathan J. |authorlink= |year=1997 |month= |title=A Pacific interdecadal climate oscillation with impacts on salmon production |journal=Bulletin of the American Meteorological Society |volume=78 |issue= 6|pages=1069–1079 |doi=10.1175/1520-0477(1997)078<1069:APICOW>2.0.CO;2 |url=http://www.atmos.washington.edu/~mantua/abst.PDO.html |accessdate= |display-authors=1 |last2=Hare |first2=Steven R. |last3=Zhang |first3=Yuan |last4=Wallace |first4=John M. |last5=Francis |first5=Robert C. |bibcode=1997BAMS...78.1069M}}</ref>
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| The prevailing hypothesis is that the PDO is caused by a "[[Brownian noise|reddening]]" of the [[El Niño–Southern Oscillation]] (ENSO) combined with [[stochastic]] atmospheric forcing.<ref name="Newman 2003">{{cite journal |last1=Newman |first1=M. |last2=Compo |first2=G.P. |last3=Alexander |title=ENSO-Forced Variability of the Pacific Decadal Oscillation |journal=[[Journal of Climate]] |volume=16 |pages=3853–3857 |year=2003 |doi=10.1175/1520-0442(2003)016<3853:EVOTPD>2.0.CO;2 |issue=23 |first3=Michael A.|bibcode = 2003JCli...16.3853N }}</ref>
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| A PDO signal has been reconstructed to 1661 through tree-ring chronologies in the [[Baja California]] area.<ref name="Biondi2001">{{cite journal |last=Biondi |first=Franco |authorlink= |coauthors=Gershunov, Alexander; Cayan, Daniel R. |year=2001 |month= |title=North Pacific Decadal Climate Variability since 1661 |journal=Journal of Climate |volume=14 |issue=1 |pages=5–10 |doi=10.1175/1520-0442(2001)014<0005:NPDCVS>2.0.CO;2 |url=http://www.ngdc.noaa.gov/paleo/pubs/biondi2001/biondi2001.html |accessdate= |bibcode=2001JCli...14....5B}}</ref>
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| The '''interdecadal Pacific oscillation''' (IPO or ID) displays similar [[ocean heat content|sea-surface temperature]] (SST) and sea-level pressure (SLP) patterns, with a cycle of 15–30 years, but affects both the north and south Pacific. In the tropical Pacific, maximum SST anomalies are found away from the equator. This is quite different from the quasi-decadal oscillation (QDO) with a period of 8-to-12 years and maximum SST anomalies straddling the equator, thus resembling the [[ENSO]].
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| == Mechanisms ==
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| Several studies have indicated that the PDO index can be reconstructed as the superimposition of tropical forcing and extra-tropical processes.<ref name="Newman 2003"/><ref name="Vimont 2005">{{cite journal |last=Vimont |first=Daniel J. |authorlink= |coauthors=|year=2005 |month= |title= The Contribution of the Interannual ENSO Cycle to the Spatial Pattern of Decadal ENSO-Like Variability|journal=Journal of Climate|volume=18 |issue=12|pages=2080–2092|doi=10.1175/JCLI3365.1|pmid=|bibcode = 2005JCli...18.2080V }}</ref><ref name="Schneider 2005">{{cite journal |last=Schneider |first=Niklas |authorlink= |coauthors=Bruce D. Cornuelle|year=2005 |month= |title= The Forcing of the Pacific Decadal Oscillation|journal=Journal of Climate|volume=18 |issue=8|pages=4355–4372|doi=10.1175/JCLI3527.1|pmid=|bibcode = 2005JCli...18.4355S }}</ref><ref name="Qiu 2007">{{cite journal |last=Qiu |first=Bo|authorlink= |coauthors=Niklas Schneider, Shuiming Chen|year=2007 |month= |title= Coupled Decadal Variability in the North Pacific: An Observationally Constrained Idealized Model|journal=Journal of Climate|volume=20 |issue=14|pages=3602–3620|doi=10.1175/JCLI4190.1 |url=http://journals.ametsoc.org/doi/full/10.1175/JCLI4190.1|accessdate=2010-09-16 |pmid=|bibcode = 2007JCli...20.3602Q }}</ref> Thus, unlike [[ENSO]], the PDO is not a single physical mode of ocean variability, but rather the sum of several processes with different dynamic origins.
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| At inter-annual time scales the PDO index is reconstructed as the sum of random and ENSO induced variability in the [[Aleutian low]], on decadal timescales ENSO teleconnections, stochastic atmospheric forcing and changes in the North Pacific oceanic [[gyre]] circulation contribute approximately equally, additionally sea surface temperature anomalies have some winter to winter persistence due to the reemergence mechanism.
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| ; ENSO teleconnections, the atmospheric bridge<ref name="Alenxander 2002">{{cite journal |last=Alexander |first=Michael A |authorlink= |coauthors=Ileana Bladé,Matthew Newman,John R. Lanzante,Ngar-Cheung Lau,James D. Scott|year=2002 |month= |title= The Atmospheric Bridge: The Influence of ENSO Teleconnections on Air–Sea Interaction over the Global Oceans|journal=Journal of Climate|volume=15 |issue=16|pages=2205–2231|doi=10.1175/1520-0442(2002)015<2205:TABTIO>2.0.CO;2|pmid=|bibcode = 2002JCli...15.2205A }}</ref>
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| [[Image:Atmospheric bridge.png|thumb|250px|right|The atmospheric bridge during el nino]]
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| ENSO can influence the global circulation pattern thousands of kilometers away from the equatorial Pacific through the "atmospheric bridge". During [[ENSO|El Nino]] events [[deep convection]] and heat transfer to the troposphere is enhanced over the anomalously warm [[sea surface temperature]], this ENSO related tropical forcing generates [[Rossby waves]] that propagates poleward and eastward and are subsequently refracted back from the pole to the tropics. The [[Rossby waves|planetary waves]] forms at preferred locations both in the North and South Pacific Ocean and the teleconnection pattern is established within 2–6 weeks.<ref name="Liu 2007">{{cite journal |last=Liu |first=Zhengyu |authorlink= |coauthors=Alexander Michael|year=2007 |month= |title= Atmospheric bridge, oceanic tunnel,and global climate teleconnections
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| |journal=Reviews of Geophysics|volume=45 |issue=2|pages=2|doi=10.1029/2005RG000172 |url=http://www.agu.org/journals/ABS/2007/2005RG000172.shtml|accessdate=2010-09-20|pmid= |bibcode=2007RvGeo..45.2005L}}</ref> ENSO driven patterns modify surface temperature,humidity, wind and the distribution of cloud over the North Pacific that alter surface heat, momentum and freshwater fluxes and thus induce sea surface temperature,salinity and [[mixed layer]] depth (MLD) anomalies.
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| The atmospheric bridge is more effective during boreal winter when the deepened [[Aleutian low]] results in stronger and cold northwesterly winds over the central Pacific and warm/humid southerly winds along the North American west coast, the associated changes in the surface heat fluxes and to a lesser extent [[Ekman transport]] creates negative sea surface temperature anomalies and a deepened MLD in the central pacific and warm the ocean from the Hawaii to the [[Bering Sea]].
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| ; SST reemergence<ref name="Deser 2003">{{cite journal |last=Deser |first=Clara |authorlink= |coauthors=Michael A. Alexander, Michael S. Timlin|year=2003|month= |title= Understanding the Persistence of Sea Surface Temperature Anomalies in Midlatitudes|journal=Journal of Climate|volume=16|issue=12|pages=57–72|doi=10.1175/1520-0442(2003)016<0057:UTPOSS>2.0.CO;2|pmid=|bibcode = 2003JCli...16...57D }}</ref>
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| {{multiple image|align=right|direction=vertical|width=250|image1=Sst_reemergence.png|thumb|caption1=Reemergence mechanism in the North Pacific.|image2=Mixed_layer_depth_seasonal_cycle.png|caption2=Mixed layer depth seasonal cycle.}}
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| Midlatitude [[Sea surface temperature|SST]] anomaly patterns tend to recur from one winter to the next but not during the intervening summer, this process occurs because of the strong [[mixed layer]] seasonal cycle. The mixed layer depth over the North Pacific is deeper, typically 100-200m, in winter than it is in summer and thus SST anomalies that forms during winter and extend to the base of the mixed layer are sequestered beneath the shallow summer mixed layer when it reforms in late spring and are effectively insulated from the air-sea heat flux. When the mixed layer deepens again in the following autumn/early winter the anomalies may influence again the surface. This process has been named "reemergence mechanism" by Alexander and Deser<ref name="Alexander 1995">{{cite journal |last=Alexander |first=Michael A. |authorlink= |coauthors=Deser Clara|year=1995|month= |title= A Mechanism for the Recurrence of Wintertime Midlatitude SST Anomalies|journal= Journal of Physical Oceanography|volume=125|issue=1 |pages=122–137 |doi=10.1175/1520-0485(1995)025<0122:AMFTRO>2.0.CO;2|pmid=|bibcode = 1995JPO....25..122A }}</ref> and is observed over much of the North Pacific Ocean although is more effective in the west where the winter mixed layer is deeper and the seasonal cycle greater.
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| ;Stochastic atmospheric forcing<ref name="Alexander 1996">{{cite journal |last=Alexander |first=Michael A. |authorlink= |coauthors=Penland, Cecile|year=1996 |month= |title=Variability in a mixed layer ocean model driven by stochastic atmospheric forcing|journal=Journal of Climate|volume=9 |issue=10|pages=2424–2442|doi=10.1175/1520-0442(1996)009<2424:VIAMLO>2.0.CO;2|pmid=|bibcode = 1996JCli....9.2424A }}</ref>
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| Long term sea surface temperature variation may be induced by random atmospheric forcings that are integrated and reddened into the ocean mixed layer. The stochastic climate model paradigm was proposed by Frankignoul and Hasselmann,<ref name="Frankignoul 1977">{{cite journal |last=Frankignoul |first=Claude |authorlink= |coauthors=Hasselmann, Klaus|year=1977 |month= |title= Stochastic climate models, Part II Application to sea-surface temperature anomalies and thermocline variability|journal=Tellus|volume=24 |issue=4|pages=289–305 |doi=10.1111/j.2153-3490.1977.tb00740.x|pmid=}}</ref> in this model a stochastic forcing represented by the passage of storms alter the ocean mixed layer temperature via surface energy fluxes and Ekman currents and the system is damped due to the enhanced (reduced) heat loss to the atmosphere over the anomalously warm (cold) SST via turbulent energy and [[longwave]] radiative fluxes, in the simple case of a linear negative [[feedback]] the model can be written as the separable [[ordinary differential equation]]:
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| <math>{\operatorname{d}y\over\operatorname{d}t}= v(t)- \lambda t</math>
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| where v is the random atmospheric forcing, λ is the damping rate (positive and constant) and y is the response.
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| The variance spectrum of y is:
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| <math>{G(w) = \frac{F}{w^2 + \lambda ^2 }}</math>
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| where F is the variance of the white noise forcing and w is the frequency, an implication of this equation is that at short time scales (w>>λ) the variance of the ocean temperature increase with the square of the period while at longer timescales(w<<λ, ~150 months) the damping process dominates and limits sea surface temperature anomalies so that the spectra became white.
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| Thus an atmospheric white noise generates SST anomalies at much longer timescales but without spectral peaks. Modeling studies suggest that this process contribute to as much as 1/3 of the PDO variability at decadal timescales.
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| ;Ocean dynamics
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| Several dynamic oceanic mechanisms and SST-air feedback may contribute to the observed decadal variability in the North Pacific Ocean. SST variability is stronger in the [[Kuroshio Current|Kuroshio]] [[oyashio current|Oyashio]] extension (KOE) region and is associated with changes in the KOE axis and strength,<ref name="Qiu 2007" /> that generates decadal and longer time scales SST variance but without the observed magnitude of the spectral peak at ~10 years, and SST-air feedback. Remote reemergence occurs in regions of strong current such as the Kuroshio extension and the anomalies created near the Japan may reemerge the next winter in the central pacific.
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| * ''' Advective resonance'''
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| Saravanan and McWilliams<ref name="Saravanan 1998">{{cite journal |last=Saravanan |first=R. |authorlink= |coauthors=McWilliams James C.|year=1998 |month= |title=Advective Ocean–Atmosphere Interaction: An Analytical Stochastic Model with Implications for Decadal Variability|journal=Journal of Climate|volume=11 |issue=2|pages=165–188|doi=10.1175/1520-0442(1998)011<0165:AOAIAA>2.0.CO;2|pmid=|bibcode = 1998JCli...11..165S }}</ref> have demonstrated that the interaction between spatially coherent atmospheric forcing patterns and an advective ocean shows periodicities at preferred time scales when non-local advective effects dominates over the local sea surface temperature damping. This "advective resonance" mechanism may generate decadal SST variability in the Eastern North Pacific associated with the anomalous Ekman advection and surface heat flux.<ref name="Wu 2003">{{cite journal |last=Wu |first=Lixin |authorlink= |coauthors=Zhengyu Liu|year=2003 |month= |title= Decadal Variability in the North Pacific: The Eastern North Pacific Mode|journal=Journal of Climate|volume=16 |issue=19|pages=3111–3131|doi=10.1175/1520-0442(2003)016<3111:DVITNP>2.0.CO;2|pmid=|bibcode = 2003JCli...16.3111W }}</ref>
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| * ''' North Pacific oceanic gyre circulation '''
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| Dynamic gyre adjustments are essential to generate decadal [[Sea surface temperature|SST]] peaks in the North Pacific, the process occurs via westward propagating oceanic [[Rossby waves]] that are forced by wind anomalies in the central and eastern Pacific Ocean. The quasigeostrophic equation for long non-dispersive Rossby Waves forced by large scale wind stress can be written as the linear [[partial differential equation]]:<ref name="Jin 1997">{{cite journal |last=Jin |first=Fei-Fei |authorlink= |coauthors=|year=1997|month= |title=A Theory of Interdecadal Climate Variability of the North Pacific Ocean–Atmosphere System|journal=Journal of Climate|volume=10 |issue=8|pages=1821–1835|doi=10.1175/1520-0442(1997)010<1821:ATOICV>2.0.CO;2|url=http://journals.ametsoc.org/doi/full/10.1175/1520-0442(1997)010%3C1821%3AATOICV%3E2.0.CO%3B2|accessdate=2010-10-07 |pmid=|bibcode = 1997JCli...10.1821J }}</ref>
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| <math>{\partial h\over\partial t} -c{\partial h\over\partial t} = \frac{-\nabla \times \vec{\tau}}{\rho_0f_0}</math>
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| where h is the upper-layer thickness anomaly, τ is the wind stress, c is the [[Rossby wave]] speed that depends on latitude, ρ<sub>0</sub> is the density of sea water and f<sub>0</sub> is the Coriolis parameter at a reference latitude. The response time scale is set by the Rossby waves speed, the location of the wind forcing and the basin width, at the latitude of the Kuroshio Extension c is 2.5 cm s<sup>−1</sup> and the dynamic gyre adjustement timescale is ~(5)10 years if the Rossby wave was initiated in the (central)eastern Pacific Ocean.
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| If the wind white forcing is zonally uniform it should generate a red spectrum in which h variance increase with the period and reaches a constant amplitude at lower frequencies without decadal and interdecadal peaks, however low frequencies atmospheric circulation tends to be dominated by fixed spatial patterns so that wind forcing is not zonally uniform, if the wind forcing is zonally sinusoidal then decadal peaks occurs due to resonance of the forced basin-scale Rossby waves.
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| The propagation of h anomalies in the western pacific changes the KOE axis and strength<ref name="Qiu 2007" /> and impact sst due to the anomalous geostrophic heat transport. Recent studies<ref name="Qiu 2007" /><ref name="Ceballos 2009">{{cite journal |last=Ceballos |first=Lina |authorlink= |coauthors=Emanuele Di Lorenzo; Carlos D. Hoyos; Niklas Schneider; Bunmei Taguchi|year=2009|month= |title=North Pacific Gyre Oscillation Synchronizes Climate Fluctuations in the Eastern and Western Boundary Systems|journal=Journal of Climate|volume=22 |issue=19|pages=5163–5174|doi=10.1175/2009JCLI2848.1|url=http://journals.ametsoc.org/doi/full/10.1175/1520-0442(1997)010%3C1821%3AATOICV%3E2.0.CO%3B2|accessdate=2010-10-07 |pmid=|bibcode = 2009JCli...22.5163C }}</ref> suggest that Rossby waves excited by the Aleutian low propagates the PDO signal from the North Pacific to the KOE through changes in the KOE axis while Rossby waves associated with the [[North Pacific Oscillation|NPO]] propagates the [[North Pacific Gyre]] oscillation signal through changes in the KOE strength.
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| == Impacts ==
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| ''' Temperatures and precipitations '''
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| {{multiple image | width = 150
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| | image1 = PDO_Temperature.png
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| | image2 = PDO Precipitation.png
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| | caption1 = PDO DJFM temperature pattern.
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| | caption2 = PDO DJFM precipitation pattern.
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| }}
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| The IPO/PDO spatial pattern and impacts are similar to those associated with [[ENSO]] events. During the positive phase the wintertime [[Aleutian low]] is deepened and shifted southward, warm/humid air is advected along the North American west coast and temperatures are higher than usual from the [[Pacific Northwest]] to Alaska but below normal in Mexico and the Southeastern United States.<ref name="Mantua2002">{{cite journal|last=Mantua|first=Nathan J.|coauthors=Hare, Steven R.|title=The Pacific Decadal Oscillation|journal=Journal of Oceanography|date=1 January 2002|volume=58|issue=1|pages=35–44|doi=10.1023/A:1015820616384|url=ftp://ftp.atmos.washington.edu/mantua/PDV/2002_Mantua_Hare_JO.pdf|accessdate=24 May 2013}}</ref> <br>
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| Winter precipitations are higher than usual in the Alaska Coast Range, Mexico and the Southwestern United States but reduced over Canada, Eastern Siberia and Australia<ref name="Mantua2002"/><ref name="power 1998">{{cite journal|last=Power|first=S.|coauthors=et al.|title=Australian temperature, Australian rainfall and the Southern Oscillation, 1910-1992: coherent variability and recent changes|journal=Australian Meteorological Magazine|year=1998|volume=47|issue=2|pages=85–101|url=http://cawcr.gov.au/bmrc/clfor/cfstaff/sbp/journal_articles/AMM_1998.pdf|accessdate=8 April 2013}}</ref> <br>
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| McCabe et al.<ref>{{cite journal|last=McCabe|first=G. J.|coauthors=Palecki, M. A.; Betancourt, J. L.|title=Pacific and Atlantic Ocean influences on multidecadal drought frequency in the United States|journal=Proceedings of the National Academy of Sciences|date=11 March 2004|volume=101|issue=12|pages=4136–4141|doi=10.1073/pnas.0306738101|url=http://wwwpaztcn.wr.usgs.gov/julio_pdf/McCabe_ea.pdf|accessdate=24 May 2013|bibcode = 2004PNAS..101.4136M }}</ref> showed that the PDO along with the [[Atlantic Multidecadal Oscillation|AMO]] strongly influence multidecadal droughts pattern in the United States, drought frequency is enhanced over much of the Northern United States during the positive PDO phase and over the Southwest United States during the negative PDO phase in both cases if the PDO is associated with a positive AMO.<br>
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| The Asian Monsoon is also affected, increased rainfall and decreased summer temperature is observed over the Indian subcontinent during the negative phase.<ref>{{cite journal|last=Krishnan|first=R.|coauthors=Sugi, M.|title=Pacific decadal oscillation and variability of the Indian summer monsoon rainfall|journal=Climate Dynamics|date=31 August 2003|volume=21|issue=3-4|pages=233–242|doi=10.1007/s00382-003-0330-8|bibcode = 2003ClDy...21..233K }}</ref>
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| {| class="wikitable"
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| |-
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| ! PDO Indicators !! PDO positive phase !! PDO negative phase
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| ! colspan="1" style="background: #c5f4be;" | Temperature
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| ! scope="row" | NW Pacific to Alaska
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| | Above average || Below average
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| |-
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| ! scope="row" | Mexico to South-East US
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| | Below average || Above average
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| |-
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| ! colspan="1" style="background: #c5f4be;" | Precipitation
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| ! scope="row" | Alaska coastal range
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| | Above average || Below average
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| |-
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| ! scope="row" | Mexico to South-Western US
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| | Above average || Below average
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| |-
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| ! scope="row" | Canada,Eastern Siberia and Australia
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| | Below average || Above average
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| |-
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| ! scope="row" | India summer monsoon
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| | Below average || Above average
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| |}
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| == Reconstructions and regime shifts ==
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| {{Multiple image|direction=vertical|align=right|image1=PDO.svg|image2=PDO1000yr.svg|width=250|caption1=Observed monthly values for the PDO (1900–feb2013).|caption2=Reconstructed PDO Index (993-1996).}}
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| The PDO index has been reconstructed using [[tree rings]] and other hydrologically sensitive [[Proxy (climate)|proxies]] from west North America and Asia.<ref name="Biondi2001" /><ref name="Shen 2006">{{cite journal |last=Shen |first=Caiming |authorlink= |coauthors=Wei-Chyung Wang; Wei Gong; Zhixin Hao|year=2006|month= |title=A Pacific Decadal Oscillation record since 1470 AD reconstructed from proxy data of summer rainfall over eastern China|journal=Geophys. Res. Lett.|volume=33 |issue=3|pages=|doi=10.1029/2005GL024804|url=http://www.agu.org/journals/ABS/2006/2005GL024804.shtml|accessdate=2010-10-26 |pmid= |bibcode=2006GeoRL..3303702S}}</ref><ref name="D'arrigo 2006">{{cite journal |last=D'arrigo|first=R. |authorlink= |coauthors=Wilson R.|year=2006|month= |title=On the Asian Expression of the PDO
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| |journal=International Journal of Climatology|volume=26 |issue=12|pages=1607–1617|doi=10.1002/joc.1326|pmid=|bibcode = 2006IJCli..26.1607D }}</ref>
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| MacDonald and Case<ref name="MacDonald 2005">{{cite journal |last=MacDonald|first=G.M. |authorlink= |coauthors=Case R.A.|year=2005|month= |title=Variations in the Pacific Decadal Oscillation over the past millennium|journal=Geophys. Res. Lett.|volume=32 |issue= 8|pages= |doi=10.1029/2005GL022478 |url=http://www.agu.org/journals/ABS/2005/2005GL022478.shtml |accessdate=2010-10-26 |pmid= |bibcode=2005GeoRL..3208703M}}</ref> reconstructed the PDO back to 993 using tree rings from [[California]] and [[Alberta]]. The index shows a 50-70 year periodicity but this is a strong mode of variability only after 1800, a persistent negative phase occurred during [[Medieval warm period|medieval times]] (993-1300) which is consistent with [[la nina]] conditions reconstructed in the tropical Pacific<ref name="Rein 2004">{{cite journal |last=Rein |first=Bert |authorlink= |coauthors=Andreas Lückge; Frank Sirocko|year=2004|month= |title=AA major Holocene ENSO anomaly during the Medieval period|journal=Geophys. Res. Lett.|volume=31 |issue=17|pages=|doi=10.1029/2004GL020161|url=http://www.agu.org/journals/ABS/2004/2004GL020161.shtml|accessdate=2010-10-26 |pmid= |bibcode=2004GeoRL..3117211R}}</ref> and multi-century droughts in the South-West United States.<ref name="Seager 2007">{{cite journal |last=Seager|first=Richard |authorlink= |coauthors=Graham, Nicholas; Herweijer, Celine; Gordon, Arnold L.; Kushnir, Yochanan; Cook, Ed|year=2007|month= |title=Blueprints for Medieval hydroclimate|journal=Quaternary Science Reviews|volume=26 |issue=19–21|pages=2322–2336|doi=10.1016/j.quascirev.2007.04.020|url=|pmid=|bibcode = 2007QSRv...26.2322S }}</ref>
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| Several regime shifts are apparent both in the reconstructions and instrumental data, during the 20th century regime shifts associated with concurrent changes in [[Sea surface temperature|SST]], [[Sea level pressure|SLP]], land precipitation and ocean cloud cover occurred in 1924/1925,1945/1946 and 1976/1977:<ref name="Deser 2004">{{cite journal |last=Deser|first=Clara|authorlink= |coauthors=Phillips, Adam S.; Hurrell, James W.|year=2004|month= |title=Pacific Interdecadal Climate Variability: Linkages between the Tropics and the North Pacific during Boreal Winter since 1900|journal=Journal of Climate|volume=17 |issue=15|pages=3109–3124|doi=10.1175/1520-0442(2004)017<3109:PICVLB>2.0.CO;2|pmid=|bibcode = 2004JCli...17.3109D }}</ref>
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| *1750: PDO displays an unusually strong oscillation.<ref name="Biondi2001" />
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| *1924/1925: PDO changed to a "warm" phase.<ref name="Deser 2004" />
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| *1945/1946: The PDO changed to a "cool" phase, the pattern of this regime shift is similar to the 1970s episode with maximum amplitude in the subarctic and subtropical front but with a greater signature near the Japan while the 1970s shift was stronger near the American west coast.<ref name="Deser 2004" /><ref name="Minobe 2005">{{cite journal |last=Minobe|first=Shoshiro|authorlink= |coauthors=Atsushi Maeda|year=2005|month= |title=A 1° monthly gridded sea-surface temperature dataset compiled from ICOADS from 1850 to 2002 and Northern Hemisphere frontal variability|journal=International Journal of Climatology|volume=25 |issue=7|pages=881–894|doi=10.1002/joc.1170|pmid=|bibcode = 2005IJCli..25..881M }}</ref>
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| *1976/1977: PDO changed to a "warm" phase.<ref name="Hare2000">{{cite journal |last=Hare |first=Steven R. |authorlink= |coauthors=Mantua, Nathan J. |year=2000 |month= |title=Empirical evidence for North Pacific regime shifts in 1977 and 1989 |journal=Progress in Oceanography |volume=47 |issue=2–4 |pages=103–145 |doi=10.1016/S0079-6611(00)00033-1 |url=|bibcode=2000PrOce..47..103H}}</ref>
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| *1988/1989:A weakening of the Aleutian low with associated SST changes was observed,<ref name="Trenberth 1994">{{cite journal |last=Trenberth|first=Kevin|authorlink= |coauthors=Hurrell, James W.|year=1994|month= |title=Decadal atmosphere-ocean variations in the Pacific|journal=Climate Dynamics|volume=9|issue=6|pages=303–319|doi= 10.1007/BF00204745 |accessdate=2010-10-26 |pmid= |bibcode=1994ClDy....9..303T}}</ref> in contrast to others regime shifts this change appears to be related to concurrent extratropical oscillation in the North Pacific and North Atlantic rather than tropical processes.<ref name="Yasunaka 2003">{{cite journal |last=Yasunaka|first=Sayaka|authorlink= |coauthors=Kimio Hanawa|year=2003|month= |title=Regime Shifts in the Northern Hemisphere SST Field: Revisited in Relation to Tropical Variations|journal=Journal of the Meteorological Society of Japan|volume=81|issue=2|pages=415–424|doi=10.2151/jmsj.81.415|url=http://www.jstage.jst.go.jp/article/jmsj/81/2/81_415/_article/-char/en|accessdate=2010-10-26 |pmid=}}</ref>
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| *1997/1998: Several changes in Sea surface temperature and marine ecosystem occurred in the North Pacific after 1997/1998, in contrast to prevailing anomalies observed after the 1970s shift. The SST declined along the United States west coast and substantial changes in the populations of [[salmon]], [[anchovy]] and [[sardine]] were observed as the PDO changed back to a cool "anchovy" phase .<ref name="Chavez 2003">{{cite journal |last=Chavez|first=Francisco P|authorlink= |coauthors= John Ryan, Salvador E. Lluch-Cota, Miguel Ñiquen C.|year=2003|month= |title=From Anchovies to Sardines and Back: Multidecadal Change in the Pacific Ocean |journal=Science|volume=299|issue=5604|pages=217–221|doi=10.1126/science.1075880 |accessdate=2010-10-26 |pmid=|bibcode = 2003Sci...299..217C }}</ref> However the spatial pattern of the SST change was different with a meridional SST seesaw in the central and western Pacific that resembled a strong shift in the North Pacific Gyre Oscillation rather than the PDO structure. This pattern dominated much of the North Pacific SST variability after 1989.<ref name="Bond 2003">{{cite journal |last=Bond|first=N.A.|authorlink= |coauthors= J. E. Overland; M. Spillane; P. Stabeno|year=2003|month= |title=Recent shifts in the state of the North Pacific|journal=Geophys. Res. Lett|volume=30|issue=23|pages=|doi=10.1029/2003GL018597 |accessdate=2010-10-26 |pmid= |bibcode=2003GeoRL..30wCLM1B}}</ref>
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| == Predictability ==
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| [[National oceanic and atmospheric administration|NOAA]]'s forecast [http://www.esrl.noaa.gov/psd/forecasts/sstlim/for1pdo.html] use a linear inverse modeling (LIM)<ref name="Alexander 2008">{{cite journal |last=Alexander |first=Michael A.|authorlink= |coauthors=Ludmila Matrosova; Cécile Penland; James D. Scott; Ping Chang|year=2008|month= |title=Forecasting Pacific SSTs: Linear Inverse Model Predictions of the PDO|journal=Journal of Climate|volume=21 |issue=2|pages=385–402|doi=10.1175/2007JCLI1849.1|pmid=|bibcode = 2008JCli...21..385A }}</ref> method to predict the PDO, LIM assumes that the PDO can be separated into a linear deterministic component and a non-linear component represented by random fluctuations.
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| Much of the LIM PDO predictability arises from ENSO and the global trend rather than extra-tropical processes and is thus limited to ~4 season, the prediction is consistent with the seasonal footprinting mechanism<ref name="Vimont 2003">{{cite journal |last=Vimont |first=Daniel J.|authorlink= |coauthors=John M. Wallace; David S. Battisti|year=2003|month= |title=The Seasonal Footprinting Mechanism in the Pacific: Implications for ENSO|journal=Journal of Climate|volume=16 |issue=16|pages=2668–2675|doi=10.1175/1520-0442(2003)016<2668:TSFMIT>2.0.CO;2|pmid=|bibcode = 2003JCli...16.2668V }}</ref> in which an optimal SST structure evolve into the ENSO mature phase 6–10 months later that subsequently impact the North Pacific Ocean SST via the atmospheric bridge.
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| Skills in predicting decadal PDO variability could arise from taking into account the impact of the externally forced<ref name="Meehl 2009">{{cite journal |last=Meehl |first=Gerard A.|authorlink= |coauthors=Aixue Hu; Benjamin D. Santer|year=2009|month= |title=The Mid-1970s Climate Shift in the Pacific and the Relative Roles of Forced versus Inherent Decadal Variability|journal=Journal of Climate|volume=22 |issue=3|pages=780–792|doi=10.1175/2008JCLI2552.1|pmid=|bibcode = 2009JCli...22..780M }}</ref> and internally generated<ref name="Mochizuki 2010">{{cite journal |last=Mochizuki |first=Takashi|authorlink= |coauthors=Masayoshi Ishii; Masahide Kimoto; Yoshimitsu Chikamotoc; Masahiro Watanabec; Toru Nozawad; Takashi T. Sakamotoa; Hideo Shiogamad; Toshiyuki Awajia; Nozomi Sugiuraa; Takahiro Toyodaa; Sayaka Yasunakac; Hiroaki Tatebea; Masato Moric|year=2010|month= |title=Pacific decadal oscillation hindcasts relevant to near-term climate prediction|journal=PNAS|volume=107|issue=5|pages=1833–1837|doi=10.1073/pnas.0906531107 |pmid=|bibcode = 2010PNAS..107.1833M }}</ref> Pacific variability.
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| == Related patterns ==
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| *ENSO tends to lead PDO/IPO cycling.
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| *Shifts in the IPO change the location and strength of ENSO activity. The [[South Pacific Convergence Zone]] moves northeast during El Niño and southwest during La Niña events. The same movement takes place during positive IPO and negative IPO phases respectively. (Folland et al., 2002)
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| *Interdecadal temperature variations in [[China]] are closely related to those of the [[North Atlantic oscillation|NAO]] and the NPO.
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| *The amplitudes of the [[North Atlantic oscillation|NAO]] and NPO increased in the 1960s and interannual variation patterns changed from 3–4 years to 8–15 years.
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| *[[Sea level rise]] is affected when large areas of water warm and expand, or cool and contract.
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| == See also ==
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| * [[California Current]]
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| * [[Hadley cell]]
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| * [[Ocean heat content]]
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| * [[Pacific-North American teleconnection pattern]]
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| * [[North Atlantic Oscillation]]
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| * [[Atlantic Multidecadal Oscillation]] (AMO)
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| == References ==
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| {{reflist|30em}}
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| == Further reading ==
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| * {{cite journal | author=LI Chongyin, HE Jinhai, ZHU Jinhong | title=A Review of Decadal/Interdecadal Climate Variation Studies in China | journal=Advances in Atmospheric Sciences | volume=21 | issue=3 | year=2004 | pages=425–436 | doi=10.1007/BF02915569|bibcode = 2004AdAtS..21..425L }}
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| * {{cite journal | author=C. K. Folland, J. A. Renwick, M. J. Salinger, A. B. Mullan | title=Relative influences of the Interdecadal Pacific Oscillation and ENSO in the South Pacific Convergence Zone | journal=Geophysical Research Letters | volume=29 | issue=13 | year=2002 | pages=21–1–21–4 |doi=10.1029/2001GL014201 |url=http://www.agu.org/journals/ABS/2002/2001GL014201.shtml | bibcode=2002GeoRL..29m..21F}}
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| * Steven R. Hare and Nathan J. Mantua, 2001. ''An historical narrative on the Pacific Decadal Oscillation, interdecadal climate variability and ecosystem impacts'', Report of a talk presented at the 20th NE Pacific Pink and Chum workshop, Seattle, WA, 22 March 2001. [http://www.iphc.washington.edu/Staff/hare/html/papers/pcworkshop/pcworkshop.pdf]
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| * Nathan J. Mantua and Steven R. Hare, 2002. ''The Pacific Decadal Oscillation'', Journal of Oceanography, Vol. 58, p. 35–44. {{doi|10.1023/A:1015820616384}} [http://jisao.washington.edu/PNWimpacts/Publications/Pub166.pdf]
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| * Kevin Ho, 2005. ''Salmon-omics: Effect of Pacific Decadal Oscillation on Alaskan Chinook Harvests and Market Price''. Columbia University. [http://www.columbia.edu/~kjh2103/Salmon-omics-PDO.pdf]
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| == External links ==
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| {{Commons category|Pacific Decadal Oscillation}}
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| *{{cite web | title=The Pacific Decadal Oscillation (PDO) | work=JISAO | url=http://www.jisao.washington.edu/pdo/ | accessdate=February 13, 2005 }}
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| *{{cite web | title=Pacific Decadal Oscillation (PDO) | work=[[Jet Propulsion Laboratory|JPL]] SCIENCE - PDO | url=http://sealevel.jpl.nasa.gov/science/pdo.html | accessdate=February 13, 2005 }}
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| {{Global warming}}
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| {{Climate oscillations}}
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| {{DEFAULTSORT:Pacific Decadal Oscillation}}
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| [[Category:Climatology]]
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| [[Category:Physical oceanography]]
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| [[Category:Climate patterns]]
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