Scaling relation B (Held, 2000; Schneider, 2006) Equalize the angular momentum conserving wind and the baroclinically critical wind Scaling relation A.

Slides:



Advertisements
Similar presentations
Decadal Variation of the Holton-Tan Effect Hua Lu, Thomas Bracegirdle, Tony Phillips, Andrew Bushell DynVar/SNAP Workshops, April, 2013, Reading,
Advertisements

Alan Robock Department of Environmental Sciences Rutgers University, New Brunswick, New Jersey USA
Weather Dynamics in Earth’s Atmosphere. An atmosphere is a blanket of a gases surrounding a planet. Earth’s atmosphere has distinct layers defined by.
Annular Modes of Extra- tropical Circulation Judith Perlwitz CIRES-CDC, University of Colorado.
Modeling the MOC Ronald J Stouffer Geophysical Fluid Dynamics Laboratory NOAA The views described here are solely those of the presenter and not of GFDL/NOAA/DOC.
AOS 101 Weather and Climate Lisha M. Roubert University of Wisconsin-Madison Department of Atmospheric & Oceanic Sciences.
Annual- and zonal-mean climate of the tropics (NCEP) Relative humidity [%] Temperature [degC] surface pressure [mb] equatorial trough subtropical high.
1 Geophysical Fluid Dynamics Laboratory Review June 30 - July 2, 2009.
The Atmospheric Circulation Response to Climate Change-like Thermal Forcings in a Simple GCM Amy H. Butler 1, David W.J. Thompson 2, & Ross Heikes 2 1.
Chapter 15 Global Circulation: Big Picture: Idealized View Ferrel cell Polar cell.
General Circulation and Kinetic Energy
General circulation in the tropics
Outline Further Reading: Detailed Notes Posted on Class Web Sites Natural Environments: The Atmosphere GG 101 – Spring 2005 Boston University Myneni L31:
General Circulation and Climate Zones Martin Visbeck DEES, Lamont-Doherty Earth Observatory
The relative contributions of radiative forcing and internal climate variability to the late 20 th Century drying of the Mediterranean region Colin Kelley,
THE HADLEY CIRCULATION (1735): global sea breeze HOT COLD Explains: Intertropical Convergence Zone (ITCZ) Wet tropics, dry poles Problem: does not account.
The General Circulation of the Atmosphere Tapio Schneider.
General Circulation of the Atmosphere René Garreaud
General Atmospheric Circulation
Solar Variability and Climate: From Mechanisms to Models
General Circulation of the Atmosphere Lisa Goddard 19 September 2006.
Sub-Saharan rainfall variability as simulated by the ARPEGE AGCM, associated teleconnection mechanisms and future changes. Global Change and Climate modelling.
1 Introduction to Isentropic Coordinates: a new view of mean meridional & eddy circulations Cristiana Stan School and Conference on “the General Circulation.
Me: Jared Persinger Atmospheric Science. Large Scale Drought : Persistent La Nina ( Cool tropical troposphere, pole-ward shifted jet.
ESS 111 – Climate & Global Change
Benjamin A. Schenkel and Robert E. 4 th WCRP International Conference on Reanalyses Department of Earth, Ocean,
Volcanic Climate Impacts and ENSO Interaction Georgiy Stenchikov Department of Environmental Sciences, Rutgers University, New Brunswick, NJ Thomas Delworth.
Past and Future Changes in Southern Hemisphere Tropospheric Circulation and the Impact of Stratospheric Chemistry-Climate Coupling Collaborators: Steven.
Figure (a-c). Latitude-height distribution of monthly mean ozone flux for the months of (a) January, (b) April and (c) July averaged over years 2000 to.
Variability on time scales of decades up to a century in a AOGCM simulation with realistic time-variable forcing Hans von Storch, Eduardo Zorita, Irene.
DARGAN M. W. FRIERSON UNIVERSITY OF WASHINGTON, DEPARTMENT OF ATMOSPHERIC SCIENCES PCC SUMMER INSTITUTE, COLLABORATORS: YEN-TING HWANG (UW), JACK.
Global Change: New Operations and Modeling Challenges Ants Leetmaa Geophysical Fluid Dynamics Laboratory National Oceanic and Atmospheric Administration.
Sahel Climate Change in the IPCC AR4 models Michela Biasutti in collaboration with : Alessandra Giannini, Adam Sobel, Isaac.
Lecture 5: Wind & effects of friction. The atmosphere is warmer in the equatorial belt than over the polar caps. These horizontal temperature gradients.
Hadley circulation extent. Halley (1686) first identified the dynamic forcing of air heating by differential heating between various latitudes on the.
INTRODUCTION DATA SELECTED RESULTS HYDROLOGIC CYCLE FUTURE WORK REFERENCES Land Ice Ocean x1°, x3° Land T85,T42,T31 Atmosphere T85,T42,T x 2.8 Sea.
Trends in Tropical Water Vapor ( ): Satellite and GCM Comparison Satellite Observed ---- Model Simulated __ Held and Soden 2006: Robust Responses.
Trends in Tropical Water Vapor ( ): Satellite and GCM Comparison Satellite Observed ---- Model Simulated __ Held and Soden 2006: Robust Responses.
Observed Recent Changes in the Tropopause Dian Seidel NOAA Air Resources Laboratory ~ Silver Spring, Maryland USA Bill Randel NCAR Atmospheric Chemistry.
The Atmosphere: Part 6: The Hadley Circulation Composition / Structure Radiative transfer Vertical and latitudinal heat transport Atmospheric circulation.
The tropics in a changing climate Chia Chou Research Center for Environmental Changes Academia Sinica October 19, 2010 NCU.
The Centre for Australian Weather and Climate Research A partnership between CSIRO and the Bureau of Meteorology Hanh Nguyen, Harry Hendon, Eun-Pa Lim,
Mechanisms that control the latitude of jet streams and surface westerlies Gang Chen (Princeton University) Isaac Held (GFDL) August 1,
Day Meridional Propagation of Global Circulation Anomalies ( A Global Convection Circulation Paradigm for the Annular Mode) Ming Cai 1 and R-C.
ENSO Influence on Atlantic Hurricanes via Tropospheric Warming Brian Tang* and David Neelin Dept. of Atmospheric and Oceanic Sciences, UCLA Institute of.
THE INFLUENCE OF THE 11-YEAR SOLAR CYCLE ON THE STRATOSPHERE BELOW 30KM: A REVIEW H. VAN LOON K. LABITZKE 2010/04/13 Pei-Yu Chueh.
Influence of the Increased SST on Baroclinic Instability Wave Activity under an Aqua Planet Condition Chihiro Kodama and Toshiki Iwasaki Graduate School.
Latitudinal effects Intensity of insolation is not the same at all latitudes Earth is roughly spherical, so insolation passing through 1 m 2 screen –Illuminates.
Decadal Variability in the Southern Hemisphere Xiaojun Yuan 1 and Emmi Yonekura 2 1 Lamont-Doherty Earth Observatory Columbia University 2 Department Environment.
Key ingredients in global hydrological response to external forcing Response to warming => Increased horizontal moisture fluxes => Poleward expansion of.
Amanda Maycock & Piers Forster
Dynamics in Earth’s Atmosphere
Climate Change Climate change scenarios of the
32nd Conference on Hurricanes and Tropical Meteorology
METO 637 Lesson 12.
Oliver Elison Timm ATM 306 Fall 2016
Widening of Tropical Belt in a Changing Climate: Model Simulations versus Observations Qiang Fu Dept. of Atmos. Sciences University of Washington.
Dynamics in Earth’s Atmosphere
Impact of the vertical resolution on Climate Simulation using CESM
Double tropopauses during idealized baroclinic life cycles
Baroclinic and barotropic annular modes
Dynamics in Earth’s Atmosphere
Non rotating planet.
The Hadley Cell continued…
The Course of Synoptic Meteorology
500 hPa height , surface pressure
Richard B. Rood (Room 2525, SRB)
Korea Ocean Research & Development Institute, Ansan, Republic of Korea
Volcanic Climate Impacts and ENSO Interaction
The Course of Synoptic Meteorology
Presentation transcript:

Scaling relation B (Held, 2000; Schneider, 2006) Equalize the angular momentum conserving wind and the baroclinically critical wind Scaling relation A (Held and Hou, 1980) (i)upper tropospheric wind is angular momentum conserving; (ii) the HC is energetically closed Expansion of the Hadley Cell under Global Warming Jian Lu 1,2 Gabriel A Vecchi 1 Thomas Reichler 3 1 GFDL/NOAA, Princeton, New Jersey 2 Visiting Scientist Program/University Corporation for Atmospheric Research/NOAA 3 Department of Meteorology, University of Utah, Salt Lake City Upper: the relationship between the tropical (20°S- 20°N) tropopause height (TTP, left); the extra-tropical (35°S-55°S and 35°N-55°N) tropopause height (ETH) with the meridional extent of the HC for 14 models. Plotted are the differences between minus , normalized by the the corresponding change in the global mean temperature. The red dots denote the multi-model ensemble mean. Lower: the Correlation coefficients between the full (blue bars) and detrended (sandy bars) time series of the HC extent and TTH (left) and ETH (right) for the 14 models from the A2 scenario.  Scaling relation B, in stead of A, applies to the variations of the HC width in the present-day.  The GHG-induced HC expansion in the A2 scenario should, at least in part, be attributed to the increased mid-latitude bulk static stability under global warming.  The ETH is strongly tied to the bulk static stability ( ) The zonal-mean mass flux streamfunction for the annual mean (left), DJF (middle) and JJA (right) seasons. The shading indicates the multi-model ensemble mean differences between and from A2 scenario, the contours References: Held, I. M., 2000, The general circulation of the atmosphere. Proc. Program in Geophysical Fluid Dynamics. Woods Hole Oceanographic Institution, Wood Hole, MA. Held, I. M. and A. Y. Hou, 1980, Nonlinear axially symmetric circulations in a nearly inviscid atmosphere, J. Atmos. Res., 37, Schneider, T., 2006, The general circulation of the atmosphere. Annu. Rev. Earth Planet. Sci., in press. Introduction The Hadley Cell (HC) plays a pivotal role in the earth’s climate by transporting energy and angular momentum poleward and by orchestrating the three dimensional tropical atmospheric circulation. Here, we investigate the response of the structure and intensity of the HC to green house gas (GHG) induced global warming by examining the A2 scenario simulations from the Fourth Assessment Report (AR4) of the Intergovernmental Panel on Climate Change (IPCC). We find that there is a robust poleward expansion and weakening of the HC across all the AR4 models and try to identify possible mechanism for this behavior.  Response of hydrological cycle  Scaling mechanisms of the HC width  Weakening of the Hadley Circulation 31 st Climate dyagnostics and Prediction Workshop, ESRL * Address of correspondence: Dr. Jian Lu, GFDL/NOAA, Princeton University Forrestal Campus, US Rout 1, Princeton, NJ Increasing GHG forcing B1A2A1B A kg/s TTHETH Left: The multi-model ensemble mean P-E in the A2 scenario. Shading indicates the difference between the first and the last 20 years of the 21 st century and the black line denotes the 0-isopleths averaged from 2001 to The right sub-panel shows the zonal mean averaged over (black) and (red). Right: Number count out of total 15 models that simulate a moistening (i.e.,  (P-E)>0) at each grid point.  The hydrological response to global warming is, overall a reinforcement of the global climatological background pattern.  Poleward expansion of the subtropical dry zone. The edges of the dry zone displace poleward by ~1° in each hemisphere for the multi-model ensemble mean of the A2 scenario. The breakdown by models and scenarios of the displacement of the northern (red) and southern (blue) edges of the subtropical dry zone (y- axis) versus the edges of the Hadley cell (x-axis). Plotted are the changes ( minus ) estimated from the B1, A1B and A2 scenarios. The open circles denote the multi-model ensemble mean values.  Dry zone versus the Hadley Cell Edge of the dry zone — latitude at which zonal- mean P-E crosses zeros near the subtropics Edge of the HC — the nodal latitude poleward of the extremum of the zonal-mean mass flux streamfunction at 500 hPa  The poleward expansion of the subtropical dry zone is strongly tied to the poleward expansion of the HC.  The magnitude of the expansion is a function of the GHG forcing.  85% (72%) of the scatter in the poleward displacement of the subtropics dry zones in the southern (northern) hemisphere can be explained by a linear relation to the displacements of the outer boundaries of the HC. contours the climatological streamfunction based on years The dots indicate the fractional change in the intensity of the HC for each of the 15 models. The intensity of the HC is defined as the difference between the maximum and minimum of the streamfunction for ANN, or the maximum (minimum) of the streamfunction for DJF (JJA) season.  The ensemble mean intensity of the Hadley Cell weakens for both the annual mean (by ~2.5%) and seasonal mean circulation (by ~6.5%).  Poleward expansion of the Hadley cell in both hemisphere, especially the winter cell.  The poleward mass transport at the upper branch of the HC tends to take a higher path than usual.