DOCSLIB.ORG

Chapter 3 IPCC WGI Fifth Assessment Report

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Chapter 3 IPCC WGI Fifth Assessment Report Second Order Draft Chapter 3 IPCC WGI Fifth Assessment Report 1 2 Chapter 3: Observations: Ocean 3 4 Coordinating Lead Authors: Monika Rhein (Germany), Stephen R. Rintoul (Australia) 5 6 Lead Authors: Shigeru Aoki (Japan), Edmo Campos (Brazil), Don Chambers (USA), Richard Feely (USA), 7 Sergey Gulev (Russia), Gregory C. Johnson (USA), Simon A. Josey (UK), Andrey Kostianoy (Russia), 8 Cecilie Mauritzen (Norway), Dean Roemmich (USA), Lynne Talley (USA), Fan Wang (China) 9 10 Contributing Authors: Michio Aoyama, Molly Baringer, Nicholas R. Bates, Timothy Boyer, Robert Byrne, 11 Sarah Cooley, Stuart Cunningham, Thierry Delcroix, Catia M. Domingues, John Dore, Scott Doney, Paul 12 Durack, Rana Fine, Melchor González-Dávila, Simon Good, Nicolas Gruber, Mark Hemer, David Hydes, 13 Masayoshi Ishii, Stanley Jacobs, Torsten Kanzow, David Karl, Alexander Kazmin, Samar Khatiwala, Joan 14 Kleypas, Kitack Lee, Eric Leuliette, Calvin Mordy, Jon Olafsson, James Orr, Alejandro Orsi, Geun-Ha Park, 15 Igor Polyakov, Sarah G. Purkey, Bo Qiu, Gilles Reverdin, Anastasia Romanou, Raymond Schmitt, Koji 16 Shimada, Lothar Stramma, Toshio Suga, Taro Takahashi, Toste Tanhua, Sunke Schmidtko, Karina von 17 Schuckmann, Doug Smith, Hans von Storch, Xiaolan Wang, Rik Wanninkhof, Susan Wijffels, Philip 18 Woodworth, Igor Yashayaev, Lisan Yu 19 20 Review Editors: Howard Freeland (Canada), Silvia Garzoli (USA), Yukihiro Nojiri (Japan) 21 22 Date of Draft: 5 October 2012 23 24 Notes: TSU Compiled Version 25 26 27 Table of Contents 28 29 Executive Summary..........................................................................................................................................3 30 3.1 Introduction ..............................................................................................................................................6 31 3.2 Changes in Ocean Temperature and Heat Content ..............................................................................6 32 3.2.1 Background: Instruments and Sampling.........................................................................................6 33 3.2.2 Upper Ocean Temperature .............................................................................................................7 34 3.2.3 Upper Ocean Heat Content.............................................................................................................8 35 3.2.4 Deep Ocean Temperature and Heat Content..................................................................................9 36 3.2.5 Conclusion ....................................................................................................................................10 37 Box 3.1: Change in Global Energy Inventory..............................................................................................10 38 3.3 Changes in Salinity and the Freshwater Budget .................................................................................11 39 3.3.1 Introduction...................................................................................................................................11 40 3.3.2 Global to Basin-Scale Trends .......................................................................................................12 41 3.3.3 Regional Changes in Salinity........................................................................................................13 42 3.3.4 Evidence for Change of the Global Water Cycle from Salinity ....................................................14 43 3.3.5 Conclusion ....................................................................................................................................15 44 3.4 Changes in Ocean Surface Fluxes .........................................................................................................15 45 3.4.1 Introduction...................................................................................................................................15 46 3.4.2 Air-Sea Heat Flux .........................................................................................................................15 47 3.4.3 Ocean Surface Precipitation and Freshwater Flux ......................................................................17 48 3.4.4 Wind Stress....................................................................................................................................18 49 3.4.5 Changes in Surface Waves............................................................................................................19 50 3.4.6 Conclusions...................................................................................................................................20 51 3.5 Changes in Water-Mass Properties and Ventilation...........................................................................20 52 3.5.1 Introduction...................................................................................................................................20 53 3.5.2 North Atlantic Deep Water (NADW) ............................................................................................20 54 3.5.3 North Pacific Intermediate Water (NPIW) and Subtropical Mode Water (STMW) .....................21 55 3.5.4 Southern Ocean.............................................................................................................................21 56 3.5.5 Conclusions...................................................................................................................................22 57 3.6 Changes in Ocean Circulation...............................................................................................................22 Do Not Cite, Quote or Distribute 3-1 Total pages: 89 Second Order Draft Chapter 3 IPCC WGI Fifth Assessment Report 1 3.6.1 Observing Ocean Circulation Variability.....................................................................................22 2 3.6.2 Wind-Driven Circulation Variability in the Pacific Ocean ..........................................................23 3 3.6.3 The Atlantic Meridional Overturning Circulation (AMOC).........................................................24 4 3.6.4 The Antarctic Meridional Overturning Circulation......................................................................26 5 3.6.5 Water Exchange Between Ocean Basins ......................................................................................26 6 3.6.6 Conclusion ....................................................................................................................................27 7 3.7 Sea Level Change, Including Extremes ................................................................................................27 8 3.7.1 Introduction and Overview of Sea Level Measurements ..............................................................27 9 3.7.2 Trends in Global Mean Sea Level and Components.....................................................................28 10 3.7.3 Regional Patterns of Sea Level Change........................................................................................30 11 3.7.4 Observations of Accelerations in GMSL.......................................................................................31 12 3.7.5 Changes in Extreme Sea Level......................................................................................................32 13 3.7.6 Conclusions...................................................................................................................................32 14 3.8 Ocean Biogeochemical Changes, Including Anthropogenic Ocean Acidification ............................34 15 3.8.1 Ocean Carbon...............................................................................................................................34 16 3.8.2 Anthropogenic Ocean Acidification..............................................................................................36 17 Box 3.2: Ocean Acidification .........................................................................................................................37 18 3.8.3 Oxygen ..........................................................................................................................................39 19 3.8.4 Regional and Long-Term Trends in Nutrient Distributions in the Oceans...................................40 20 3.8.5 Summary........................................................................................................................................40 21 3.9 Synthesis ..................................................................................................................................................41 22 FAQ 3.1: Is the Ocean Warming?.................................................................................................................42 23 FAQ 3.2: How Does Anthropogenic Ocean Acidification Relate to Climate Change?............................44 24 FAQ 3.3: Is There Evidence for Changes in the Earth’s Water Cycle?....................................................45 25 References........................................................................................................................................................47 26 Figures .............................................................................................................................................................62 27 28 Do Not Cite, Quote or Distribute 3-2 Total pages: 89 Second Order Draft Chapter 3 IPCC WGI Fifth Assessment Report 1 Executive
Load more

Recommended publications
  • Influences of the Choice of Climatology on Ocean Heat
    388 JOURNAL OF ATMOSPHERIC AND OCEANIC TECHNOLOGY VOLUME 32 Influences of the Choice of Climatology on Ocean Heat Content Estimation LIJING CHENG AND JIANG ZHU International Center for Climate and Environment Sciences, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing, China (Manuscript received 30 August 2014, in final form 9 October 2014) ABSTRACT The choice of climatology is an essential step in calculating the key climate indicators, such as historical ocean heat content (OHC) change. The anomaly field is required during the calculation and is obtained by subtracting the climatology from the absolute field. The climatology represents the ocean spatial variability and seasonal circle. This study found a considerable weaker long-term trend when historical climatologies (constructed by using historical observations within a long time period, i.e., 45 yr) were used rather than Argo- period climatologies (i.e., constructed by using observations during the Argo period, i.e., since 2004). The change of the locations of the observations (horizontal sampling) during the past 50 yr is responsible for this divergence, because the ship-based system pre-2000 has insufficient sampling of the global ocean, for instance, in the Southern Hemisphere, whereas this area began to achieve full sampling in this century by the Argo system. The horizontal sampling change leads to the change of the reference time (and reference OHC) when the historical-period climatology is used, which weakens the long-term OHC trend. Therefore, Argo-period climatologies should be used to accurately assess the long-term trend of the climate indicators, such as OHC. 1. Introduction methodology.
    [Show full text]
  • World Ocean Thermocline Weakening and Isothermal Layer Warming
    applied sciences Article World Ocean Thermocline Weakening and Isothermal Layer Warming Peter C. Chu * and Chenwu Fan Naval Ocean Analysis and Prediction Laboratory, Department of Oceanography, Naval Postgraduate School, Monterey, CA 93943, USA; [email protected] * Correspondence: [email protected]; Tel.: +1-831-656-3688 Received: 30 September 2020; Accepted: 13 November 2020; Published: 19 November 2020 Abstract: This paper identifies world thermocline weakening and provides an improved estimate of upper ocean warming through replacement of the upper layer with the fixed depth range by the isothermal layer, because the upper ocean isothermal layer (as a whole) exchanges heat with the atmosphere and the deep layer. Thermocline gradient, heat flux across the air–ocean interface, and horizontal heat advection determine the heat stored in the isothermal layer. Among the three processes, the effect of the thermocline gradient clearly shows up when we use the isothermal layer heat content, but it is otherwise when we use the heat content with the fixed depth ranges such as 0–300 m, 0–400 m, 0–700 m, 0–750 m, and 0–2000 m. A strong thermocline gradient exhibits the downward heat transfer from the isothermal layer (non-polar regions), makes the isothermal layer thin, and causes less heat to be stored in it. On the other hand, a weak thermocline gradient makes the isothermal layer thick, and causes more heat to be stored in it. In addition, the uncertainty in estimating upper ocean heat content and warming trends using uncertain fixed depth ranges (0–300 m, 0–400 m, 0–700 m, 0–750 m, or 0–2000 m) will be eliminated by using the isothermal layer.
    [Show full text]
  • Significant Dissipation of Tidal Energy in the Deep Ocean Inferred from Satellite Altimeter Data
    letters to nature 3. Rein, M. Phenomena of liquid drop impact on solid and liquid surfaces. Fluid Dynamics Res. 12, 61± water is created at high latitudes12. It has thus been suggested that 93 (1993). much of the mixing required to maintain the abyssal strati®cation, 4. Fukai, J. et al. Wetting effects on the spreading of a liquid droplet colliding with a ¯at surface: experiment and modeling. Phys. Fluids 7, 236±247 (1995). and hence the large-scale meridional overturning, occurs at 5. Bennett, T. & Poulikakos, D. Splat±quench solidi®cation: estimating the maximum spreading of a localized `hotspots' near areas of rough topography4,16,17. Numerical droplet impacting a solid surface. J. Mater. Sci. 28, 963±970 (1993). modelling studies further suggest that the ocean circulation is 6. Scheller, B. L. & Bous®eld, D. W. Newtonian drop impact with a solid surface. Am. Inst. Chem. Eng. J. 18 41, 1357±1367 (1995). sensitive to the spatial distribution of vertical mixing . Thus, 7. Mao, T., Kuhn, D. & Tran, H. Spread and rebound of liquid droplets upon impact on ¯at surfaces. Am. clarifying the physical mechanisms responsible for this mixing is Inst. Chem. Eng. J. 43, 2169±2179, (1997). important, both for numerical ocean modelling and for general 8. de Gennes, P. G. Wetting: statics and dynamics. Rev. Mod. Phys. 57, 827±863 (1985). understanding of how the ocean works. One signi®cant energy 9. Hayes, R. A. & Ralston, J. Forced liquid movement on low energy surfaces. J. Colloid Interface Sci. 159, 429±438 (1993). source for mixing may be barotropic tidal currents.
    [Show full text]
  • Sustained Global Ocean Observing Systems
    Introduction Goal The ocean, which covers 71 percent of the Earth’s surface, The goal of the Climate Observation Division’s Ocean Climate exerts profound influence on the Earth’s climate system by Observation Program2 is to build and sustain the in situ moderating and modulating climate variability and altering ocean component of a global climate observing system that the rate of long-term climate change. The ocean’s enormous will respond to the long-term observational requirements of heat capacity and volume provide the potential to store 1,000 operational forecast centers, international research programs, times more heat than the atmosphere. The ocean also serves and major scientific assessments. The Division works toward as a large reservoir for carbon dioxide, currently storing 50 achieving this goal by providing funding to implementing times more carbon than the atmosphere. Eighty-five percent institutions across the nation, promoting cooperation of the rain and snow that water the Earth comes directly from with partner institutions in other countries, continuously the ocean, while prolonged drought is influenced by global monitoring the status and effectiveness of the observing patterns of ocean temperatures. Coupled ocean-atmosphere system, and providing overall programmatic oversight for interactions such as the El Niño-Southern Oscillation (ENSO) system development and sustained operations. influence weather and storm patterns around the globe. Sea level rise and coastal inundation are among the Importance of Ocean Observations most significant impacts of climate change, and abrupt Ocean observations are critical to climate and weather climate change may occur as a consequence of altered applications of societal value, including forecasts of droughts, ocean circulation.
    [Show full text]
  • Causes of Sea Level Rise
    FACT SHEET Causes of Sea OUR COASTAL COMMUNITIES AT RISK Level Rise What the Science Tells Us HIGHLIGHTS From the rocky shoreline of Maine to the busy trading port of New Orleans, from Roughly a third of the nation’s population historic Golden Gate Park in San Francisco to the golden sands of Miami Beach, lives in coastal counties. Several million our coasts are an integral part of American life. Where the sea meets land sit some of our most densely populated cities, most popular tourist destinations, bountiful of those live at elevations that could be fisheries, unique natural landscapes, strategic military bases, financial centers, and flooded by rising seas this century, scientific beaches and boardwalks where memories are created. Yet many of these iconic projections show. These cities and towns— places face a growing risk from sea level rise. home to tourist destinations, fisheries, Global sea level is rising—and at an accelerating rate—largely in response to natural landscapes, military bases, financial global warming. The global average rise has been about eight inches since the centers, and beaches and boardwalks— Industrial Revolution. However, many U.S. cities have seen much higher increases in sea level (NOAA 2012a; NOAA 2012b). Portions of the East and Gulf coasts face a growing risk from sea level rise. have faced some of the world’s fastest rates of sea level rise (NOAA 2012b). These trends have contributed to loss of life, billions of dollars in damage to coastal The choices we make today are critical property and infrastructure, massive taxpayer funding for recovery and rebuild- to protecting coastal communities.
    [Show full text]
  • Chapter 2: Ocean Observations
    Chapter 2. Ocean observations 2.1 Observational methods With the rapid advancement in technology, the instruments and methods for measuring oceanic circulation and properties have been quickly evolving. Nevertheless, it is useful to understand what types of instruments have been available at different points in oceanographic development and their resolution, precision, and accuracy. The majority of oceanographic measurements so far have been made from research vessels, with auxiliary measurements from merchant ships and coastal stations. Fig. 2.1 Research vessel. Accuracy: The difference between a result obtained and the true value. Precision: Ability to measure consistently within a given data set (variance in the measurement itself due to instrument noise). Generally the precision of oceanographic measurements is better than the accuracy. 2.1.1 Measurements of depth. Each oceanographic variable, such as temperature (T), salinity (S), density , and current , is a function of space and time, and therefore a function of depth. In order to determine to which depth an instrument has been deployed, we need to measure ``depth''. Depth measurements are often made with the measurements of other properties, such as temperature, salinity and current. Meter wheel. The wire is passed over a meter wheel, which is simply a pulley of known circumference with a counter attached to the pulley to count the number of turns, thus giving the depth the instrument is lowered. This method is accurate when the sea is calm with negligible currents. In reality, research vessels are moving and currents might be strong, and thus the wire is not straight. The real depth is shorter than the distance the wire paid out.
    [Show full text]
  • The Contribution of Wind-Generated Waves to Coastal Sea-Level Changes
    1 Surveys in Geophysics Archimer November 2011, Volume 40, Issue 6, Pages 1563-1601 https://doi.org/10.1007/s10712-019-09557-5 https://archimer.ifremer.fr https://archimer.ifremer.fr/doc/00509/62046/ The Contribution of Wind-Generated Waves to Coastal Sea-Level Changes Dodet Guillaume 1, *, Melet Angélique 2, Ardhuin Fabrice 6, Bertin Xavier 3, Idier Déborah 4, Almar Rafael 5 1 UMR 6253 LOPSCNRS-Ifremer-IRD-Univiversity of Brest BrestPlouzané, France 2 Mercator OceanRamonville Saint Agne, France 3 UMR 7266 LIENSs, CNRS - La Rochelle UniversityLa Rochelle, France 4 BRGMOrléans Cédex, France 5 UMR 5566 LEGOSToulouse Cédex 9, France *Corresponding author : Guillaume Dodet, email address : [email protected] Abstract : Surface gravity waves generated by winds are ubiquitous on our oceans and play a primordial role in the dynamics of the ocean–land–atmosphere interfaces. In particular, wind-generated waves cause fluctuations of the sea level at the coast over timescales from a few seconds (individual wave runup) to a few hours (wave-induced setup). These wave-induced processes are of major importance for coastal management as they add up to tides and atmospheric surges during storm events and enhance coastal flooding and erosion. Changes in the atmospheric circulation associated with natural climate cycles or caused by increasing greenhouse gas emissions affect the wave conditions worldwide, which may drive significant changes in the wave-induced coastal hydrodynamics. Since sea-level rise represents a major challenge for sustainable coastal management, particularly in low-lying coastal areas and/or along densely urbanized coastlines, understanding the contribution of wind-generated waves to the long-term budget of coastal sea-level changes is therefore of major importance.
    [Show full text]
  • Model-Based Evidence of Deep-Ocean Heat Uptake During Surface-Temperature Hiatus Periods Gerald A
    LETTERS PUBLISHED ONLINE: XX MONTH XXXX | DOI: 10.1038/NCLIMATE1229 Model-based evidence of deep-ocean heat uptake during surface-temperature hiatus periods Gerald A. Meehl1*, Julie M. Arblaster1,2, John T. Fasullo1, Aixue Hu1 and Kevin E. Trenberth1 1 There have been decades, such as 2000–2009, when the atmosphere and land, to melt ice or snow, or to be deposited in the 50 2 observed globally averaged surface-temperature time series subsurface ocean and manifested as changes in ocean temperatures 51 1 3 shows little positive or even slightly negative trend (a hiatus and thus heat content. Changes to the cryosphere and land 52 4 period). However, the observed energy imbalance at the subsurface play a much smaller role than the atmosphere and oceans 53 5 5 top-of-atmosphere for this recent decade indicates that a in energy flows , and they are not further considered in this paper. 54 −2 6 net energy flux into the climate system of about 1 W m The time series of globally averaged surface temperature from 55 7 (refs2,3) should be producing warming somewhere in the all five climate-model simulations show some decades with little 56 4,5 8 system . Here we analyse twenty-first-century climate-model or no positive trend (Fig.1a), as has occurred in observations 57 9 simulations that maintain a consistent radiative imbalance at (Supplementary Fig. S1 top). Running ten year linear trends of 58 −2 10 the top-of-atmosphere of about 1 W m as observed for the globally averaged surface temperature from the five model ensemble 59 11 past decade.
    [Show full text]
  • Guidelines Towards an Integrated Ocean Observation System for Ecosystems and Biogeochemical Cycles
    GUIDELINES TOWARDS AN INTEGRATED OCEAN OBSERVATION SYSTEM FOR ECOSYSTEMS AND BIOGEOCHEMICAL CYCLES Hervé Claustre(1), David Antoine(1), Lars Boehme(2), Emmanuel Boss(3), Fabrizio D’Ortenzio(1), Odile Fanton D’Andon(4), Christophe Guinet(5), Nicolas Gruber(6), Nils Olav Handegard(7), Maria Hood(8), Ken Johnson(9), Arne Körtzinger(10), Richard Lampitt(11), Pierre-Yves LeTraon(12), Corinne Lequéré(13), Marlon Lewis(14), Mary-Jane Perry(15), Trevor Platt(16), Dean Roemmich(17), Shubha Sathyendranath(16), Uwe Send(17), Pierre Testor(18), Jim Yoder(19) (1) CNRS and University P. & M. Curie, Laboratoire d’Océanographie de Villefranche, 06230 Villefranche-sur-mer, France, Email: [email protected], [email protected], [email protected] (2) NERC Sea Mammal Research Unit, Scottish Oceans Institute, University of St Andrews, St Andrews, Fife KY16 8LB, Scotland, UK, Email: [email protected] (3) University of Maine, School of Marine Science, Orono, ME 04469 USA, Email: [email protected] (4) ACRI-ST, 260, route du Pin Montard - B.P. 234, 06904 Sophia Antipolis Cedex, France, Email: [email protected] (5) CNRS, Centre d'Etudes Biologiques de Chizé, Villiers-en-Bois, 79360 Beauvoir-sur-niort , France, [email protected] (6) Institute of Biogeochemistry and Pollutant Dynamics, ETH Zurich, Universitatstrasse 16, 8092 Zurich, Switzerland, Email: [email protected] (7) Institute of Marine Research, Postboks 1870 Nordnes, 5817 Bergen, Norway, Email: [email protected] (8) UNESCO-IOC, 1 Rue Miollis, 75732 Paris cedex 15, France, Email: [email protected] (9) Monterey Bay Aquarium Research Institute 7700 Sandholdt Road Moss Landing, CA 95039, USA, Email: [email protected] (10) Leibniz-Institut für Meereswissenschaften (IFM-GEOMAR) Chemische Ozeanographie Düsternbrooker Weg 20, 24105 Kiel, Germany.
    [Show full text]
  • Climate-Change–Driven Accelerated Sea-Level Rise Detected in the Altimeter Era
    Climate-change–driven accelerated sea-level rise detected in the altimeter era R. S. Nerema,1, B. D. Beckleyb, J. T. Fasulloc, B. D. Hamlingtond, D. Mastersa, and G. T. Mitchume aColorado Center for Astrodynamics Research, Ann and H. J. Smead Aerospace Engineering Sciences, Cooperative Institute for Research in Environmental Sciences, University of Colorado, Boulder, CO 80309; bStinger Ghaffarian Technologies Inc., NASA Goddard Space Flight Center, Greenbelt, MD 20771; cNational Center for Atmospheric Research, Boulder, CO 80305; dOld Dominion University, Norfolk, VA 23529; and eCollege of Marine Science, University of South Florida, St. Petersburg, FL 33701 Edited by Anny Cazenave, Centre National d’Etudes Spatiales, Toulouse, France, and approved January 9, 2018 (received for review October 2, 2017) Using a 25-y time series of precision satellite altimeter data from GMSL acceleration estimate by 0.033 mm/y2, resulting in a final TOPEX/Poseidon, Jason-1, Jason-2, and Jason-3, we estimate the “climate-change–driven” acceleration of 0.084 mm/y2. Climate- climate-change–driven acceleration of global mean sea level over change–driven in this case means we have tried to adjust the the last 25 y to be 0.084 ± 0.025 mm/y2. Coupled with the average GMSL measurements for as many natural interannual and decadal climate-change–driven rate of sea level rise over these same 25 y of effects as we can to try to isolate the longer-term, potentially an- 2.9 mm/y, simple extrapolation of the quadratic implies global mean thropogenic, acceleration––any remaining effects are considered in sea level could rise 65 ± 12 cm by 2100 compared with 2005, roughly the error analysis.
    [Show full text]
  • The Ocean, a Heat Reservoir
    ocean-climate.org The ocean, Sabrina Speich a heat reservoir The ocean’s ability to store heat (uptake of 94% of the excess energy resulting from increased atmospheric concentration of greenhouse gases due to human activities) is much more efficient than that of the continents (2%), ice (2%) or the atmosphere (2%) (Figure 1; Bindoff et al., 2007; Rhein et al., 2013; Cheng et al., 2019). It thus has a moderating effect on climate and climate change. However, ocean uptake of the excess heat generated by an increase in atmospheric greenhouse gas concentrations causes marine waters to warm up, which, in turn, affects the ocean's properties, dynamics, volume, and exchanges with the atmosphere (including rainfall cycle and extreme events) and marine ecosystem habitats. For a long time, discussions on climate change did not take the oceans into account, simply because we knew very little about them. However, our ability to understand and anticipate changes in the Earth’s climate depends on our detailed knowledge of the oceans and their relationship to the climate. THE OCEAN: A HEAT RESERVOIR CO2 emissions (Le Quéré et al., 2018). Without the ocean, AND WATER SOURCE the atmospheric warming observed since the early 19th century would be much more intense. Earth is the only known planet where water is present in its three states (liquid, gas and solid) and in particular in Our planet’s climate is governed to a significant extent liquid form in the ocean. Due to the high heat capacity by the ocean, which is its primary regulator thanks to the of water, its radiative properties and phase changes, ocean's ability to fully absorb any kind of incident radia- the ocean is largely responsible for the mildness of our tion on its surface and its continuous radiative, mechani- planet’s climate and for water inflows to the continents, cal and gaseous exchanges with the atmosphere.
    [Show full text]
  • Argo and Ocean Heat Content: Progress and Issues
    Argo and Ocean Heat Content: Progress and Issues Dean Roemmich, Scripps Ins2tu2on of Oceanography, USA, October 2013, CERES Mee2ng Outline • What makes Argo different from 20th century oceanography? • Issues for heat content es2maon: measurement errors, coverage bias, the deep ocean. • Regional and global ocean heat gain during the Argo era, 2006 – 2013. How do Argo floats work? Argo floats collect a temperature and salinity profile and a trajectory every 10 days, with data returned by satellite and made available within 24 hours via 20 min on sea surface the GTS and internet (hXp://www.argo.net) . Collect T/S profile on 9 days dri_ing ascent 1000 m Temperature Salinity Map of float trajectory Temperature/Salinity relation 2000 m Cost of an Argo T,S profile is ~ $170. Typical cost of a shipboard CTD profile ~$10,000. Argo’s 1,000,000th profile was collected in late 2012, and 120,000 profiles are being added each year. Global Oceanography Argo AcCve Argo floats Global-scale Oceanography All years, Non-Argo T,S Float technology improvements New generaon floats (SOLO-II, Navis, ARVOR, NOVA) • Profile 0-2000 dbar anywhere in the world ocean. • Use Iridium 2-way telecoms: – Short surface 2me (15 mins) greatly reduces surface divergence, grounding, bio-fouling, damage. – High ver2cal resolu2on (2 dbar full profile). – Improved surface layer sampling (1 dbar resolu2on, with pump cutoff at 1 dbar). • Lightweight (18 kg) for shipping and deployment. • Increased baery life for > 300 cycles (6 years @ 7-days). SIO Deep SOLO SOLO-II, WMO ID 5903539 (le_), deployed 4/2011. Note strong (10 cm/s) annual veloci2es at 1000 m This Deep SOLO completed 65 cycles to 4000 m and is rated to 6000 m.
    [Show full text]