Observed and Expected Changes to the Tropical Pacific Ocean

Total Page:16

File Type:pdf, Size:1020Kb

Observed and Expected Changes to the Tropical Pacific Ocean Photo: Bruno Marty / IRD Chapter 3 Observed and expected changes to the tropical Pacific Ocean Alexandre S Ganachaud, Alex Sen Gupta, James C Orr, Susan E Wijffels, Ken R Ridgway, Mark A Hemer, Christophe Maes, Craig R Steinberg, Aline D Tribollet, Bo Qiu and Jens C Kruger ‘The oceans are warming.’ (Bindoff et al. 2007)i L %LQGRIIHWDO 2EVHUYDWLRQV2FHDQLFFOLPDWHFKDQJHDQGVHDOHYHO,Q66RORPRQ'4LQ 00DQQLQJ=&KHQ00DUTXLV.%$YHU\W07LJQRUDQG+/0LOOHU HGV &OLPDWH &KDQJH 7KH3K\VLFDO6FLHQFH%DVLV&RQWULEXWLRQRI:RUNLQJ*URXS,WRWKH)RXUWK$VVHVVPHQW5HSRUWRI WKH,QWHUJRYHUQPHQWDO3DQHORQ&OLPDWH&KDQJH&DPEULGJH8QLYHUVLW\3UHVV&DPEULGJH8QLWHG .LQJGRPDQG1HZ<RUN8QLWHG6WDWHVRI$PHULFDSS² 101 Contents Page 3.1 Introduction 103 3.1.1 Use of climate simulations 104 3.2 Features of the tropical Pacific Ocean 105 3.2.1 Large-scale currents 105 3.2.2 Ocean temperature 110 3.2.3 Ocean eddies 120 3.2.4 Nutrient supply 123 3.2.5 Dissolved oxygen 127 3.2.6 Ocean acidification 129 3.2.7 Wave height 131 3.2.8 Sea level 135 3.2.9 Coastal circulation and island effects 137 3.3 Observed and projected changes in the tropical Pacific Ocean 141 3.3.1 Large-scale currents 141 3.3.2 Ocean temperature 143 3.3.3 Ocean eddies 149 3.3.4 Nutrient supply 150 3.3.5 Dissolved oxygen 157 3.3.6 Ocean acidification 159 3.3.7 Wave height 163 3.3.8 Sea level 164 3.3.9 Coastal circulation and island effects 167 3.4 Summary of present-day ocean features, and observed and projected changes 169 3.5 Recommendations to reduce uncertainties in projecting future changes to the tropical Pacific Ocean 172 3.5.1 SPCZ and ENSO 172 3.5.2 Integrating biogeochemical and physical models 173 3.5.3 Dynamical downscaling 173 3.5.4 Long-term observations and monitoring 173 References 176 Appendix 188 102 CHAPTER 3 3.1 Introduction 7KHÀVKDQGLQYHUWHEUDWHVKDUYHVWHGIURPWKHWURSLFDO3DFLÀF2FHDQDQGWKHFRDVWDO ZDWHUVRIWKHUHJLRQDQGWKHHFRV\VWHPVWKDWVXSSRUWWKHVHVSHFLHVDUHLQÁXHQFHG QRWRQO\E\VXUIDFHFOLPDWHWKH\DOVRGHSHQGLQWLPDWHO\RQWKHRFHDQLFHQYLURQPHQW /DUJHDQGVPDOOVFDOHFLUFXODWLRQSDWWHUQVLQÁXHQFHODUYDOGLVSHUVDODQGWKH PLJUDWLRQ RI VSHFLHV ZDWHU WHPSHUDWXUH VDOLQLW\ QXWULHQW DYDLODELOLW\ GLVVROYHG R[\JHQFRQFHQWUDWLRQDQGS+DIIHFWELRORJLFDODFWLYLW\DQGRFHDQLFFXUUHQWVZDYHV DQGVHDOHYHOVKDSHFRDVWDOKDELWDWV7RJHWKHUWKHVHSURSHUWLHVRIWKHWURSLFDO3DFLÀF 2FHDQLLKDYHDSURIRXQGHIIHFWRQWKHSURGXFWLYLW\RIRFHDQLFDQGFRDVWDOÀVKHULHV DQGFRDVWDODTXDFXOWXUH 8QGHUVWDQGLQJKRZWKHVHIHDWXUHVRIWKHRFHDQYDU\LVRQHRIWKHSULPDU\NH\VWR IRUHFDVWLQJSURGXFWLRQIURPWKHÀVKHULHVVHFWRU5HVROYLQJWKLVSX]]OHLVDPDMRU FKDOOHQJHKRZHYHUEHFDXVHWKHWURSLFDO3DFLÀF2FHDQYDULHVDFURVV DQ HQRUPRXV UDQJHRIVSDWLDODQGWHPSRUDOVFDOHV)RUH[DPSOHZLWKLQMXVWDIHZGD\VFORXGFRYHU ORFDOXSZHOOLQJVXUIDFHPL[LQJGXHWRVWRUPVRURFHDQLFHGGLHVFDQVXEVWDQWLDOO\ PRGLI\VHDVXUIDFHWHPSHUDWXUHVDOLQLW\FXUUHQWVDQGQXWULHQWVXSSO\DWWKHVFDOH RIUHHIVDQGLVODQGV2QODUJHUVSDWLDOVFDOHVVHDVRQDOFKDQJHVLQQXWULHQWXSZHOOLQJ KDYHDVLJQLÀFDQWHIIHFWRQSULPDU\SURGXFWLYLW\ &KDSWHU &ORVHUWRWKHHTXDWRU NH\SURSHUWLHVRIWKH3DFLÀF2FHDQDUHGRPLQDWHGE\WKHLQWHUDQQXDOYDULDWLRQVRIWKH (O1LxR6RXWKHUQ2VFLOODWLRQ (162 &KDSWHU 2QORQJHUWLPHVFDOHVYDULDWLRQVLQ WKHVWUHQJWKRIWKHPLGODWLWXGHZHVWHUO\ZLQGVSURGXFHFOLPDWH¶UHJLPHVKLIWV·OLNH WKRVHUHFRUGHGLQDQGDQGLQ²5HJLPHVKLIWVDUHFKDUDFWHULVHG E\DEUXSW(162OLNHFKDQJHVWKDWFDQODVWIRUVHYHUDOGHFDGHVFRPPRQO\DVVRFLDWHG ZLWKWKH,QWHUGHFDGDO3DFLÀF2VFLOODWLRQ ,32 RUWKHFORVHO\UHODWHG3DFLÀF'HFDGDO 2VFLOODWLRQ 3'2 ²3URIRXQGFKDQJHVRYHUDQGDERYHQDWXUDOFOLPDWHYDULDELOLW\DUH DOVRRFFXUULQJGXHWRWKHEXLOGXSRIDQWKURSRJHQLFJUHHQKRXVHJDVHPLVVLRQVLQWKH DWPRVSKHUH &KDSWHUVDQG 7KH SXUSRVH RI WKLV FKDSWHU LV WR SURYLGH ÀVKHULHV VFLHQWLVWV DQG PDQDJHUV ZLWK IXQGDPHQWDO LQIRUPDWLRQ RQ WKH PDLQ IHDWXUHV RI WKH WURSLFDO 3DFLÀF 2FHDQ KRZ WKHVH IHDWXUHV KDYH FKDQJHG RYHU WKH SDVW IHZ GHFDGHV GXH WR FOLPDWH FKDQJH &KDSWHU DQGKRZWKH\DUHSURMHFWHGWRFKDQJHDVWKHOHYHOVRI&2LQFUHDVHDQG WKHHDUWKFRQWLQXHVWRZDUP 7KH RFHDQLF IHDWXUHV ZH H[DPLQH LQFOXGH ODUJHVFDOH FXUUHQWV VHD VXUIDFH WHPSHUDWXUH DQG VDOLQLW\ VXEVXUIDFH WHPSHUDWXUH HGGLHV QXWULHQWV GLVVROYHG R[\JHQRFHDQDFLGLÀFDWLRQZDYHKHLJKWVHDOHYHOULVHDQGFRDVWDODQGLVODQGHIIHFWV LL 'HÀQHGDVWKHDUHD1WR6DQG(WR: 103 3.1.1 Use of climate simulations 7R GHVFULEH WKH IHDWXUHV RI WKH WURSLFDO 3DFLÀ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² PHDQVWDWHRIWKH RFHDQDQGDVVHVVHGWKHDELOLW\RIWKHPRGHOVWRUHSURGXFH(162OLNHEHKDYLRXU²WKH GRPLQDQWGULYHURILQWHUDQQXDOYDULDELOLW\LQWKHUHJLRQ &KDSWHU 7RGRWKLVZH DQDO\VHGWKHVWUHQJWKVSDWLDOVWUXFWXUHDQGWHPSRUDOFKDUDFWHULVWLFVRIWKHVLPXODWHG (162LQFRQMXQFWLRQZLWKWKHUHVXOWVIURPSUHYLRXVVWXGLHV² $VGLVFXVVHGLQ&KDSWHUZKLOHPRVWPRGHOVUHSURGXFHVRPHIRUPRI(162OLNH YDULDELOLW\WKHOHYHORIUHDOLVPGLIIHUVPDUNHGO\$IHZIRUH[DPSOHSURGXFHDQ (162WKDWRFFXUVDOPRVWHYHU\VHFRQG\HDU7KHUHDUHDOVRFRQVLGHUDEOHGLIIHUHQFHV LQWKHVWUHQJWKDQGVHDVRQDOLW\RIDQRPDOLHVLQVHDVXUIDFHWHPSHUDWXUH2IPDMRU FRQFHUQLVDV\VWHPDWLFELDVLQWKHVSDWLDOVWUXFWXUHRI(162LQDOPRVWDOOWKHPRGHOV ZKHUHE\WKHPD[LPXPZDUPLQJWKDWRFFXUVGXULQJ(O1LxRHYHQWVLVGLVSODFHGWRR IDUWRWKHZHVW$VDUHVXOWZHUHWDLQHGRIWKH&0,3PRGHOV $SSHQGL[ WKDW H[KLELWHG(162OLNHEHKDYLRXUZLWKDGRPLQDQWIUHTXHQF\EHWZHHQDQG\HDUV DQGDUHDVRQDEOHUHSUHVHQWDWLRQRIWKH:DUP3RROLQWKHZHVWHUQ3DFLÀF &KDSWHU (YHQDIWHUPRGHOVHOHFWLRQVRPHELDVHVSHUVLVWHG:KHUHWKHVHELDVHVGLGQRWRFFXU DFURVVDODUJHQXPEHURIPRGHOVZHXVHGWKH¶PXOWLPRGHOPHDQ·WR¶DYHUDJHRXW· PDQ\RIWKHELDVHVLQLQGLYLGXDOPRGHOV7KLVDYHUDJLQJSURFHVVJHQHUDOO\ JLYHVD FRQVLVWHQWO\ PRUH UHDOLVWLF UHSUHVHQWDWLRQ RI WKH UHDO ZRUOG WKDQDQ\LQGLYLGXDO PRGHO &KDSWHU EXWPDVNVWKHSRVVLELOLW\RIPRUHH[WUHPHFKDQJHV:HXVHGWKH PXOWLPRGHOPHDQWRSURYLGHWKHEHVWHVWLPDWHRI WKHSUHVHQWVWDWHRIWKHWURSLFDO 3DFLÀF2FHDQFHQWUHGRQ ² DQG IXWXUHSURMHFWLRQV IRU WKH PDLQ IHDWXUHVRIWKHRFHDQGHVFULEHGDERYHRILQWHUHVWWRÀVKHULHVLQWKHWURSLFDO3DFLÀF $VRXWOLQHGLQ&KDSWHUZHFRQVLGHUHGWKHIXWXUHSURMHFWLRQVIRUERWKDUHODWLYHO\ ORZHPLVVLRQV % DQGDUHODWLYHO\KLJKHPLVVLRQV $ VFHQDULRIRUDQG7R WKLVHQGZHXVHG\HDUVHJPHQWVRIHDFKPRGHO·VRXWSXWIRUWR KHUHDIWHU UHIHUUHGWRDV DQGWR KHUHDIWHUUHIHUUHGWRDV LLL UHVSHFWLYHO\ WRGHÀQHDPHDQFOLPDWHDQGWRDYHUDJHRXWDQ\VKRUWWHUPYDULDELOLW\0RVWRIWKH GLDJQRVWLFVDUHEDVHGRQWKHPHDQRIWKHVHOHFWHGVXEVHWRIFOLPDWHPRGHOV PXOWL PRGHO PHDQ 6WXGHQW V WWHVWV ZHUH XVHG WR GHWHUPLQH ZKHWKHU WKH FOLPDWHGULYHQ LLL 6RPHJOREDOFOLPDWHPRGHOVRQO\PDNHSURMHFWLRQVWRVRZHKDYHXVHGWKH\HDUSHULRG ²WRUHSUHVHQW 104 CHAPTER 3 FKDQJHV LQ RFHDQLF IHDWXUHV FRXOG EH FRQVLGHUHG WR EH VWDWLVWLFDOO\ VLJQLÀFDQW $OWKRXJK VRPH ORQJWHUP PXOWLGHFDGDO WR PLOOHQQLDO YDULDELOLW\PD\EHSUHVHQW LQWKHVLPXODWLRQVUHVXOWLQJLQDELDVLQPHDQVWDWHHVWLPDWHV WKLV LV HVVHQWLDOO\ UHPRYHGE\XVLQJWKHPXOWLPRGHOPHDQ 3.2 Features of the tropical Pacific Ocean 3.2.1 Large-scale currents %RWK ODUJH DQG VPDOOVFDOH FXUUHQWV SOD\ D PDMRU UROH LQ WKH GLVWULEXWLRQ DQG DEXQGDQFHRIÀVKDQGLQYHUWHEUDWHVWKDWVXSSRUWWKHRFHDQLFDQGFRDVWDOÀVKHULHVRI WKHWURSLFDO3DFLÀ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ÁXHQFHWKHUHSOHQLVKPHQWRINH\VSHFLHVVXSSRUWLQJFRDVWDOÀVKHULHV DWWKHHQGRIWKHLUSHODJLFSKDVHSRVWODUYDHRIÀVKDQGLQYHUWHEUDWHVXVHFXUUHQWVWR ÀQGWKHKDELWDWVRQZKLFKWKH\GHSHQGDVDGXOWV &KDSWHU 3.2.1.1 Currents flowing into the region 7KHPDLQFXUUHQWVLQWKHWURSLFDO3DFLÀF2FHDQ )LJXUH DUHGULYHQE\WKHHDVWHUO\ WUDGH ZLQGV &KDSWHU 7KH SULPDULO\ ZHVWZDUG ÁRZ RI WKHVH FXUUHQWV H[WHQGV RYHUWKHWRSIHZKXQGUHGPHWUHVRIWKHRFHDQDQGUHDFKHVWKHZHVWHUQERXQGDU\RI WKH EDVLQ ,Q WKH ÀUVW IHZ WHQV RI PHWUHV DQ LQWHUDFWLRQ EHWZHHQWKH&RULROLVIRUFH DVVRFLDWHGZLWKWKHURWDWLRQRIWKHHDUWK DQGWKHWUDGHZLQGVFDXVH¶(NPDQWUDQVSRUW· %R[ ZKHUHWKHVXUIDFHZDWHUVLQWKHWURSLFVPRYHSROHZDUGLQERWKKHPLVSKHUHV &RQYHUVHO\ DW ODWLWXGHV SROHZDUG RI 1 DQG 6 WKH SUHYDLOLQJ ZHVWHUO\ ZLQGV IRUFHWKHVXUIDFHZDWHUVWRZDUGVWKHHTXDWRUUHVXOWLQJLQDFRQYHUJHQFH RI WKHVH ZDWHUVEHWZHHQ²1DQG²67KLVFRQYHUJHQFHSURGXFHVDEXLOGXS LQVHDVXUIDFHKHLJKW 66+ DURXQG²1WR²67KHVHDOHYHO VORSH LV DVVRFLDWHGZLWKSUHVVXUHIRUFHVWKDWGULYHWZREURDGJHRVWURSKLF ZHVWZDUG ÁRZV %R[ WKH1RUWK(TXDWRULDO&XUUHQW 1(& DQGWKH6RXWK(TXDWRULDO&XUUHQW 6(& )LJXUHE 7KH1(&DQG6(&DUHWKHHTXDWRULDOEUDQFKHVRIWZREDVLQVFDOHFLUFXODU FLUFXODWLRQSDWWHUQVWKHODUJHVXEWURSLFDOJ\UHVLQWKHQRUWKHUQDQGVRXWKHUQ3DFLÀF 2FHDQZLWKWKHLUSROHZDUGPDUJLQVRXWVLGHWKHGRPDLQDWKLJKHUODWLWXGHV1HDUWKH VXUIDFH ²P IULFWLRQDOIRUFHVIURPWKHZLQGDUHVXSHULPSRVHGRQWKHJHRVWURSKLF 1(&DQG6(&DGGLQJDFRPSRQHQWWKDWLVSHUSHQGLFXODUWRWKHORFDOZLQGGLUHFWLRQ GXHWR(NPDQWUDQVSRUW VHHEOXHVWUHDPOLQHVVKRZLQJ(NPDQFXUUHQWVLQ)LJXUH )RU H[DPSOH VRXWK RI WKH HTXDWRU WKH VRXWKHDVWHUO\ WUDGH ZLQGV EHQG WKH VXUIDFH VWUHDPOLQHVWRWKHVRXWKZHVW 105 a) 120°E 140°E 160°E 180° 160°W 140°W 20°N 10°N 0° 10°S 20°S 0 10
Recommended publications
  • Cross-Shelf Transport of Pink Shrimp Larvae: Interactions of Tidal Currents, Larval Vertical Migrations and Internal Tides
    Vol. 345: 167–184, 2007 MARINE ECOLOGY PROGRESS SERIES Published September 13 doi: 10.3354/meps06916 Mar Ecol Prog Ser Cross-shelf transport of pink shrimp larvae: interactions of tidal currents, larval vertical migrations and internal tides Maria M. Criales1,*, Joan A. Browder2, Christopher N. K. Mooers1, Michael B. Robblee3, Hernando Cardenas1, Thomas L. Jackson2 1Rosenstiel School of Marine and Atmospheric Science, University of Miami, 4600 Rickenbacker Causeway, Miami, Florida 33149, USA 2NOAA Fisheries, Southeast Fisheries Science Center, 75 Virginia Beach Drive, Miami, Florida 33149, USA 3US Geological Survey, Center for Water and Restoration Studies, 3110 SW 9th Avenue, Ft Lauderdale, Florida 33315, USA ABSTRACT: Transport and behavior of pink shrimp Farfantepenaeus duorarum larvae were investi- gated on the southwestern Florida (SWF) shelf of the Gulf of Mexico between the Dry Tortugas spawning grounds and Florida Bay nursery grounds. Stratified plankton samples and hydrographic data were collected at 2 h intervals at 3 stations located on a cross-shelf transect. At the Marquesas station, midway between Dry Tortugas and Florida Bay, internal tides were recognized by anom- alously cool water, a shallow thermocline with strong density gradients, strong current shear, and a high concentration of pink shrimp larvae at the shallow thermocline. Low Richardson numbers occurred at the pycnocline depth, indicating vertical shear instability and possible turbulent transport from the lower to the upper layer where myses and postlarvae were concentrated. Analysis of verti- cally stratified plankton suggested that larvae perform vertical migrations and the specific behavior changes ontogenetically; protozoeae were found deeper than myses, and myses deeper than postlar- vae.
    [Show full text]
  • I. Wind-Driven Coastal Dynamics II. Estuarine Processes
    I. Wind-driven Coastal Dynamics Emily Shroyer, Oregon State University II. Estuarine Processes Andrew Lucas, Scripps Institution of Oceanography Variability in the Ocean Sea Surface Temperature from NASA’s Aqua Satellite (AMSR-E) 10000 km 100 km 1000 km 100 km www.visibleearth.nasa.Gov Variability in the Ocean Sea Surface Temperature (MODIS) <10 km 50 km 500 km Variability in the Ocean Sea Surface Temperature (Field Infrared Imagery) 150 m 150 m ~30 m Relevant spatial scales range many orders of magnitude from ~10000 km to submeter and smaller Plant DischarGe, Ocean ImaginG LanGmuir and Internal Waves, NRL > 1000 yrs ©Dudley Chelton < 1 sec < 1 mm > 10000 km What does a physical oceanographer want to know in order to understand ocean processes? From Merriam-Webster Fluid (noun) : a substance (as a liquid or gas) tending to flow or conform to the outline of its container need to describe both the mass and volume when dealing with fluids Enterà density (ρ) = mass per unit volume = M/V Salinity, Temperature, & Pressure Surface Salinity: Precipitation & Evaporation JPL/NASA Where precipitation exceeds evaporation and river input is low, salinity is increased and vice versa. Note: coastal variations are not evident on this coarse scale map. Surface Temperature- Net warming at low latitudes and cooling at high latitudes. à Need Transport Sea Surface Temperature from NASA’s Aqua Satellite (AMSR-E) www.visibleearth.nasa.Gov Perpetual Ocean hWp://svs.Gsfc.nasa.Gov/cGi-bin/details.cGi?aid=3827 Es_manG the Circulaon and Climate of the Ocean- Dimitris Menemenlis What happens when the wind blows on Coastal Circulaon the surface of the ocean??? 1.
    [Show full text]
  • Coastal Upwelling Revisited: Ekman, Bakun, and Improved 10.1029/2018JC014187 Upwelling Indices for the U.S
    Journal of Geophysical Research: Oceans RESEARCH ARTICLE Coastal Upwelling Revisited: Ekman, Bakun, and Improved 10.1029/2018JC014187 Upwelling Indices for the U.S. West Coast Key Points: Michael G. Jacox1,2 , Christopher A. Edwards3 , Elliott L. Hazen1 , and Steven J. Bograd1 • New upwelling indices are presented – for the U.S. West Coast (31 47°N) to 1NOAA Southwest Fisheries Science Center, Monterey, CA, USA, 2NOAA Earth System Research Laboratory, Boulder, CO, address shortcomings in historical 3 indices USA, University of California, Santa Cruz, CA, USA • The Coastal Upwelling Transport Index (CUTI) estimates vertical volume transport (i.e., Abstract Coastal upwelling is responsible for thriving marine ecosystems and fisheries that are upwelling/downwelling) disproportionately productive relative to their surface area, particularly in the world’s major eastern • The Biologically Effective Upwelling ’ Transport Index (BEUTI) estimates boundary upwelling systems. Along oceanic eastern boundaries, equatorward wind stress and the Earth s vertical nitrate flux rotation combine to drive a near-surface layer of water offshore, a process called Ekman transport. Similarly, positive wind stress curl drives divergence in the surface Ekman layer and consequently upwelling from Supporting Information: below, a process known as Ekman suction. In both cases, displaced water is replaced by upwelling of relatively • Supporting Information S1 nutrient-rich water from below, which stimulates the growth of microscopic phytoplankton that form the base of the marine food web. Ekman theory is foundational and underlies the calculation of upwelling indices Correspondence to: such as the “Bakun Index” that are ubiquitous in eastern boundary upwelling system studies. While generally M. G. Jacox, fi [email protected] valuable rst-order descriptions, these indices and their underlying theory provide an incomplete picture of coastal upwelling.
    [Show full text]
  • The Role of Ekman Ocean Heat Transport in the Northern Hemisphere Response to ENSO
    The Role of Ekman Ocean Heat Transport in the Northern Hemisphere Response to ENSO Michael A. Alexander NOAA/Earth System Research Laboratory, Boulder, Colorado, USA James D. Scott CIRES, University of Colorado, and NOAA/ Earth System Research Laboratory, Boulder, Colorado. Submitted to the Journal of Climate December 2007 Corresponding Author Michael Alexander NOAA/Earth System Research Laboratory Physical Science Division R/PSD1 325 Broadway Boulder, Colorado 80305 [email protected] 1 Abstract The role of oceanic Ekman heat transport (Qek) on air-sea variability associated with ENSO teleconnections is examined via a pair of atmospheric general circulation model (AGCM) experiments. In the “MLM” experiment, observed sea surface temperatures (SSTs) for the years 1950-1999 are specified over the tropical Pacific, while a mixed layer model is coupled to the AGCM elsewhere over the global oceans. The same experimental design was used in the “EKM” experiment with the addition of Qek in the mixed layer ocean temperature equation. The ENSO signal was evaluated using differences between composites of El Niño and La Niña events averaged over the 16 ensemble members in each experiment. In both experiments the Aleutian Low deepened and the resulting surface heat fluxes cooled the central North Pacific and warmed the northeast Pacific during boreal winter in El Niño relative to La Niña events. Including Qek increased the magnitude of the ENSO- related SST anomalies by ~1/3 in the central and northeast North Pacific, bringing them close to the observed ENSO signal. Differences between the ENSO-induced atmospheric circulation anomalies in the EKM and MLM experiments were not significant over the North Pacific.
    [Show full text]
  • Oceanography Lecture 12
    Because, OF ALL THE ICE!!! Oceanography Lecture 12 How do you know there’s an Ice Age? i. The Ocean/Atmosphere coupling ii.Surface Ocean Circulation Global Circulation Patterns: Atmosphere-Ocean “coupling” 3) Atmosphere-Ocean “coupling” Atmosphere – Transfer of moisture to the Low latitudes: Oceans atmosphere (heat released in higher latitudes High latitudes: Atmosphere as water condenses!) Atmosphere-Ocean “coupling” In summary Latitudinal Differences in Energy Atmosphere – Transfer of moisture to the atmosphere: Hurricanes! www.weather.com Amount of solar radiation received annually at the Earth’s surface Latitudinal Differences in Salinity Latitudinal Differences in Density Structure of the Oceans Heavy Light T has a much greater impact than S on Density! Atmospheric – Wind patterns Atmospheric – Wind patterns January January Westerlies Easterlies Easterlies Westerlies High/Low Pressure systems: Heat capacity! High/Low Pressure systems: Wind generation Wind drag Zonal Wind Flow Wind is moving air Air molecules drag water molecules across sea surface (remember waves generation?): frictional drag Westerlies If winds are prolonged, the frictional drag generates a current Easterlies Only a small fraction of the wind energy is transferred to Easterlies the water surface Westerlies Any wind blowing in a regular pattern? High/Low Pressure systems: Wind generation by flow from High to Low pressure systems (+ Coriolis effect) 1) Ekman Spiral 1) Ekman Spiral Once the surface film of water molecules is set in motion, they exert a Spiraling current in which speed and direction change with frictional drag on the water molecules immediately beneath them, depth: getting these to move as well. Net transport (average of all transport) is 90° to right Motion is transferred downward into the water column (North Hemisphere) or left (Southern Hemisphere) of the ! Speed diminishes with depth (friction) generating wind.
    [Show full text]
  • Storm Surge Reduction by Mangroves
    Natural Coastal Protection Series ISSN 2050-7941 Storm Surge Reduction by Mangroves Anna McIvor, Tom Spencer, Iris Möller and Mark Spalding Natural Coastal Protection Series: Report 2 Cambridge Coastal Research Unit Working Paper 41 Authors: Anna L. McIvor, The Nature Conservancy, Cambridge, UK and Cambridge Coastal Research Unit, Department of Geography, University of Cambridge, UK. Corresponding author: [email protected] Tom Spencer, Cambridge Coastal Research Unit, Department of Geography, University of Cambridge, UK. Iris Möller, Cambridge Coastal Research Unit, Department of Geography, University of Cambridge, UK. Mark Spalding, The Nature Conservancy, Cambridge, UK and Department of Zoology, University of Cambridge, UK. Published by The Nature Conservancy and Wetlands International in 2012. The Nature Conservancy’s Natural Coastal Protection project is a collaborative work to review the growing body of evidence as to how, and under what conditions, natural ecosystems can and should be worked into strategies for coastal protection. This work falls within the Coastal Resilience Program, which includes a broad array of research and action bringing together science and policy to enable the development of resilient coasts, where nature forms part of the solution. The Mangrove Capital project aims to bring the values of mangroves to the fore and to provide the knowledge and tools necessary for the improved management of mangrove forests. The project advances the improved management and restoration of mangrove forests as an effective strategy for ensuring resilience against natural hazards and as a basis for economic prosperity in coastal areas. The project is a partnership between Wetlands International, The Nature Conservancy, Deltares, Wageningen University and several Indonesian partner organisations.
    [Show full text]
  • Physical Oceanography - UNAM, Mexico Lecture 3: the Wind-Driven Oceanic Circulation
    Physical Oceanography - UNAM, Mexico Lecture 3: The Wind-Driven Oceanic Circulation Robin Waldman October 17th 2018 A first taste... Many large-scale circulation features are wind-forced ! Outline The Ekman currents and Sverdrup balance The western intensification of gyres The Southern Ocean circulation The Tropical circulation Outline The Ekman currents and Sverdrup balance The western intensification of gyres The Southern Ocean circulation The Tropical circulation Ekman currents Introduction : I First quantitative theory relating the winds and ocean circulation. I Can be deduced by applying a dimensional analysis to the horizontal momentum equations within the surface layer. The resulting balance is geostrophic plus Ekman : I geostrophic : Coriolis and pressure force I Ekman : Coriolis and vertical turbulent momentum fluxes modelled as diffusivities. Ekman currents Ekman’s hypotheses : I The ocean is infinitely large and wide, so that interactions with topography can be neglected ; ¶uh I It has reached a steady state, so that the Eulerian derivative ¶t = 0 ; I It is homogeneous horizontally, so that (uh:r)uh = 0, ¶uh rh:(khurh)uh = 0 and by continuity w = 0 hence w ¶z = 0 ; I Its density is constant, which has the same consequence as the Boussinesq hypotheses for the horizontal momentum equations ; I The vertical eddy diffusivity kzu is constant. ¶ 2u f k × u = k E E zu ¶z2 that is : k ¶ 2v u = zu E E f ¶z2 k ¶ 2u v = − zu E E f ¶z2 Ekman currents Ekman balance : k ¶ 2v u = zu E E f ¶z2 k ¶ 2u v = − zu E E f ¶z2 Ekman currents Ekman balance : ¶ 2u f k × u = k E E zu ¶z2 that is : Ekman currents Ekman balance : ¶ 2u f k × u = k E E zu ¶z2 that is : k ¶ 2v u = zu E E f ¶z2 k ¶ 2u v = − zu E E f ¶z2 ¶uh τ = r0kzu ¶z 0 with τ the surface wind stress.
    [Show full text]
  • Ocean Surface Circulation
    Ocean surface circulation Recall from Last Time The three drivers of atmospheric circulation we discussed: • Differential heating • Pressure gradients • Earth’s rotation (Coriolis) Last two show up as direct forcing of ocean surface circulation, the first indirectly (it drives the winds, also transport of heat is an important consequence). Coriolis In northern hemisphere wind or currents deflect to the right. Equator In the Southern hemisphere they deflect to the left. Major surfaceA schematic currents of them anyway Surface salinity A reasonable indicator of the gyres 31.0 30.0 32.0 31.0 31.030.0 33.0 33.0 28.0 28.029.0 29.0 34.0 35.0 33.0 33.0 33.034.035.0 36.0 34.0 35.0 37.0 35.036.0 36.0 34.0 35.0 35.0 35.0 34.0 35.0 37.0 35.0 36.0 36.0 35.0 35.0 35.0 34.0 34.0 34.0 34.0 34.0 34.0 Ocean Gyres Surface currents are shallow (a few hundred meters thick) Driving factors • Wind friction on surface of the ocean • Coriolis effect • Gravity (Pressure gradient force) • Shape of the ocean basins Surface currents Driven by Wind Gyres are beneath and driven by the wind bands . Most of wind energy in Trade wind or Westerlies Again with the rotating Earth: is a major factor in ocean and Coriolisatmospheric circulation. • It is negligible on small scales. • Varies with latitude. Ekman spiral Consider the ocean as a Wind series of thin layers. Friction Direction of Wind friction pushes on motion the top layers.
    [Show full text]
  • Persistence of Coastal Upwelling After a Plunge in Upwelling-Favourable
    www.nature.com/scientificreports OPEN Persistence of coastal upwelling after a plunge in upwelling‑favourable wind Jihun Jung & Yang‑Ki Cho* Unprecedented coastal upwelling of the southern coast of the Korean Peninsula was reported during the summer of 2013. The upwelling continued for more than a month after a plunge in upwelling- favourable winds and had serious impacts on fsheries. This is a rare phenomenon, as most coastal upwelling events relax a few days after the wind weakens. In this study, observational data and numerical modelling results were analysed to investigate the cause of the upwelling and the reason behind it being sustained for such an extended period. Coastal upwelling was induced by an upwelling- favourable wind in July, resulting in the dynamic uplift of deep, cold water. The dynamic uplift decreased the steric sea level in the coastal region. The sea level diference between the coastal and ofshore regions produced an intensifed cross-shore pressure gradient that enhanced the surface geostrophic current along the coast. The strong surface current maintained the dynamic uplift due to geostrophic equilibrium. This positive feedback between the dynamic uplift and geostrophic adjustment sustained the coastal upwelling for a month following a plunge in the upwelling‑ favourable wind. Coastal upwelling is a process that brings deep, cold water to the ocean surface. It can play an important role both in physical processes and in chemical and biological variability in coastal regions by transporting nutri- ents to the surface layer. Coastal upwelling can be induced by various mechanisms, but it generally results from Ekman transport due to the alongshore wind stress1,2.
    [Show full text]
  • Physical and Biogeochemical Processes Associated with Upwelling in the Indian Ocean Puthenveettil Narayan
    https://doi.org/10.5194/bg-2020-486 Preprint. Discussion started: 9 February 2021 c Author(s) 2021. CC BY 4.0 License. 1 Reviews and syntheses: Physical and biogeochemical processes associated with upwelling in the 2 Indian Ocean 1* 2 3 4 3 Puthenveettil Narayana Menon Vinayachandran , Yukio Masumoto , Mike Roberts , Jenny Hugget , 5 6 7 8 9 4 Issufo Halo , Abhisek Chatterjee , Prakash Amol , Garuda V. M. Gupta , Arvind Singh , Arnab 10 6 11 12 13 5 Mukherjee , Satya Prakash , Lynnath E. Beckley , Eric Jorden Raes , Raleigh Hood 6 7 1Centre for Atmospheric and Oceanic Sciences, Indian Institute of Science, Bengaluru, 560012, India 8 9 2 Graduate School of Science, University of Tokyo, Tokyo, Japan 10 11 3 Nelson Mandela University, Port Elizabeth, South Africa 12 13 4Oceans and Coasts Research, Department of Environment, Forestry and Fisheries, Private Bag X4390, Cape Town 8000, 14 South Africa 15 16 5Department of Conservation and Marine Sciences, Cape Peninsula University of Technology, PO Box 652, Cape Town 17 8000, South Africa 18 6Indian National Centre for Indian Ocean Services, Ministry of Earth Sciences, Hyderabad, India 19 20 7CSIR-National Institute of Oceanography, Regional Centre, Visakhapatnam, 530017, India 21 22 8Centre for Marine Living Resources and Ecology, Ministry of Earth Sciences, Kochi, India 23 24 9Physical Research Laboratory, Ahmedabad, 380009, India 25 26 10 National Centre for Polar and Ocean Research, Ministry of Earth Sciences, Goa, India 27 28 11 Environmental and Conservation Sciences, Murdoch University, Perth, Western Australia 6150, Australia 29 30 12 CSIRO Oceans and Atmosphere, GPO Box 1538, Hobart, TAS, 7001 Australia 31 32 13 University of Maryland Center for Environmental Science, Cambridge, MD, USA 33 34 *Correspondence to: P.
    [Show full text]
  • Ekman Transport in Balanced Currents with Curvature
    MAY 2017 W E N E G R A T A N D T H O M A S 1189 Ekman Transport in Balanced Currents with Curvature JACOB O. WENEGRAT AND LEIF N. THOMAS Department of Earth System Science, Stanford University, Stanford, California (Manuscript received 24 October 2016, in final form 6 March 2017) ABSTRACT Ekman transport, the horizontal mass transport associated with a wind stress applied on the ocean surface, is modified by the vorticity of ocean currents, leading to what has been termed the nonlinear Ekman transport. This article extends earlier work on this topic by deriving solutions for the nonlinear Ekman transport valid in currents with curvature, such as a meandering jet or circular vortex, and for flows with the Rossby number approaching unity. Tilting of the horizontal vorticity of the Ekman flow by the balanced currents modifies the ocean response to surface forcing, such that, to leading order, winds parallel to the flow drive an Ekman transport that depends only on the shear vorticity component of the vertical relative vorticity, whereas across- flow winds drive transport dependent on the curvature vorticity. Curvature in the balanced flow field thus leads to an Ekman transport that differs from previous formulations derived under the assumption of straight flows. Notably, the theory also predicts a component of the transport aligned with the surface wind stress, contrary to classic Ekman theory. In the case of the circular vortex, the solutions given here can be used to calculate the vertical velocity to a higher order of accuracy than previous solutions, extending possible ap- plications of the theory to strong balanced flows.
    [Show full text]
  • The United States Virgin Islands 8 Tyler B
    The United States Virgin Islands 8 Tyler B. Smith, Marilyn E. Brandt, Viktor W. Brandtneris, Rosmin S. Ennis, Sarah H. Groves, Sennai Habtes, Daniel M. Holstein, Elizabeth Kadison, and Richard S. Nemeth Abstract (45–151 species), but often their biomass is dominated by Mesophotic coral ecosystems (MCEs) at 30–100 m depth a few species, particularly on edges with high abundances are the dominant hard bottom habitat in the US Virgin of planktivores and piscivores. Despite their importance to Islands of the northeastern Caribbean Sea. Well-developed­ the ecology and economy of USVI, MCEs are threatened MCEs surpass the extent of shallow coral reefs by almost by a variety of local and global stressors and disturbances a factor of three. These habitats range from high coral that are causing declines in coral cover. cover structural reefs to low coral cover hard bottoms on banks, slopes, and walls. The most common communities Keywords in the United States Virgin Islands (USVI) are star coral Mesophotic coral ecosystems · Orbicella banks · (Orbicella franksi) banks that are concentrated in a rela- Agaricia fringe · Fish spawning aggregations · tively large area (187 km2) south and southwest of St. Disturbance Thomas in depths of 30–43 m. Wall and slope coral com- munities in upper (30–60 m) and lower MCE (60–100 m) depths are dominated by lettuce corals (Agaricia spp.) Most MCEs are heavily covered in macroalgae, particu- 8.1 Introduction larly Lobophora variegata. Corals are species rich in many upper MCE habitats (20–28 species) compared with shal- Caribbean mesophotic coral ecosystems (MCEs) are hard low reefs (31), but not in upper and lower MCE slopes and bottom habitats containing or dominated by scleractinian walls (6–8).
    [Show full text]