THE TENDENCY OF CLIMATE CHANGE OVER THE PAST SEVERAL MILLIONS OF YEARS AND THE CURRENT INTERGLACIAL DURATION. V.A. Dergachev
|
|
- Bertram Barber
- 5 years ago
- Views:
Transcription
1 THE TENDENCY OF CLIMATE CHANGE OVER THE PAST SEVERAL MILLIONS OF YEARS AND THE CURRENT INTERGLACIAL DURATION V.A. Dergachev Ioffe Physical-Technical Institute, St. Petersburg, , Russia, Abstract. The Earth's climate, from regional to global, varies on all time scales. Large-scale climate variations in the past can be related to changes in geological processes (plate tectonic) and orbital cycles upon the Earth s climate. Astronomical theories of paleoclimate attribute climate cycles to changes in the Earth s orbital parameters: eccentricity (~100 kyr), obliquity (~41 kyr), precession (~22 kyr). It has been established from the paleoclimate and paleo-oceanographic data that during last more than 50 millions of years planetary temperatures were several degrees warmer than today, but there has been a progressive decrease in the average surface temperature on this time interval. Substantial glacial and interglacial temperature fluctuations are imposed on this decrease since about 2.8 million years ago. The last interglacial peak (at ~130 kyr ago) was a period with significantly higher temperatures in many parts of the Northern Hemisphere compared to the currant interglacial period, which started ~ 11,000 years ago. A detailed analysis of the recent oscillations in temperature shows a clear 100,000 year correlation with the interglacial periods coinciding with the maxima of the elipticity of the Earth s orbit. To understand better our current interglacial period (the Holocene, MIS-1 [Marine Isotope Stage]) and its future, it is necessary to investigate the response of the climate system to the peaks of interglacials in the past. Start of the last interglacial period occured at ~130 kyr ago (MIS-5). Similar to the Holocene, the latitudinal and seasonal distributions of the incoming solar radiation show two interglacials: MIS 11 (start kyr ago) and MIS 19 (start kyr ago). However, it is difficult to find in the available climate data a complete analogue to the current interglacial climate. The available data on climatic changes and the cyclic influence of solar radiation on the climate change are analyzed and the problem of current interglacial duration is discussed. Introduction The climate of the distant past (the first billion years of the Earth existence), where geological records are almost non-existent or sparse, is very poorly understood. During the evolution of our planet its climate was characterized by a large variety of climate stages. There were periods of increased variability or regular oscillations or almost quiet phases. Over the entire time coverage of the Earth s history the main external and internal natural mechanisms of climate variability are related to changes in plate tectonics, orbital changes with different periodicities, the sun s output on different time scales, and volcanism. Natural climate variability in the past was the rule and not the exception and the evolution of life on Earth was closely linked to climate and its change. The usual definition of climate is that it includes the slowly varying aspects of the atmosphere hydrosphere surface system. Let's look at the climate change over longer (millions and thousands of years) time scales. It has been established from the paleoclimate and paleo-oceanographic data (Zachos et al., 2001) that during the past 100 million of years in the Cretaceous epoch, which ended 65 Myr BP (Figure 1), surface air temperatures were higher than they are at present. Since about 65 million years ago, Earth s climate has undergone a significant cooling and complex evolution. About 55 million years ago, at the end of the Paleocene, there was a sudden warming event in which temperatures rose by about 6ºC globally and by 10-20ºC at the poles (Zachos et al., 2008). Hansen et al. (2011) showed that the deep-sea temperature is closely related to the global average temperature and they roughly estimated that the change in global average temperature was perhaps ~ 12 o C over the past 50 million years. The Earth s climate has cooled over the last 5 million years. Today, mankind is living in an interglacial period that began about 11 ky ago. In the light of discussion about global warming observed in recent decades, which advocates an anthropogenic impact associated with the emission of greenhouse gases due to combustion of fossil fuel, the question concerning the duration of the current interglacial arises. The available data on climate change and solar radiation on a time scale of the last millions of years are critically analyzed and the problem of the length of the current interglacial is discussed. 245
2 Figure 1. Climate during the Cenozoic Era (~10 8 foraminifers (Zachos et al., 2001). years). Oxygen isotope measurements of benthic Climate changes over the past and orbital cycles One of the highest resolution records of global proxy temperature data over the last 5.3 million years was published by Lisiecki and Raymo [2005] (Figure 2a). This set consists of a stack of 57 globally distributed benthic δ 18 O records. The data are based on samples of deep sea sediments consisting of calcium carbonate from plankton. As one can see from Figure 2, the Earth s climate has cooled down over the last 5 million years. The data provide overwhelming evidence for a major cooling trend. The cooling culminated in the Pleistocene glaciation, which began about 2.5 Myr ago. As a result, the Earth s climate has been marked by temperature swings between extended glacial periods, leading to a series of major glaciations over the last 900,000 years, which were characterized by thick ice sheets covering large parts of North America, Northern Europe and Siberia, and interglacial times characterized by the ice coverage only in Antarctica and sometimes Greenland, as at the present time. Figure 2. a - δ 18 O benthic stack over the past 5 Myr [Lisiecki and Raymo, 2005]. b - Local wavelet power spectra of δ 18 O data derived using a modified version of the WTC-16 code [Grinsted et al., 2004]. Shaded areas show the cone-of-interference, within which edge effects become significant. The data were smoothed to 5 kyr resolution before wavelet decomposition [Russon et al., 2011], which limits the capacity of the method to resolved periodicities <20 kyr. The causes of glacial interglacial climate changes can be linked to solar activity or to processes occurring on earth. Since major climate changes have a cyclic character, the astronomical theory, proposed by 246
3 Milankovitch [1948], relates glacial interglacial changes to changes in the Earth s orbit and its rotation axis in time. Theory suggests that a primary driver of ice ages is the total summer radiation received in northern latitude zones where major ice sheets have being formed in the past, near 65 degrees of Northern latitudes. A spectral analysis (Figure 2b) of the data supports this relationship up to a certain degree. These climatic data clearly show a certain kind of periodic variability. The main orbital periodicities are the precession (~20 kyr), eccentricity (~100 kyr and ~400 kyr) and obliquity (~40 kyr) cycles (Laskar et al., 2004). The combined effect of these orbital cycles causes long term changes in the amount of sunlight hitting the Earth in different seasons, particularly at high latitudes. The data of δ 18 O exhibit the cycles 20, 41 and 100 kyr (Figure 2b), which coincide with the orbital periodicities mentioned above. Climate variability during the last three million years, on the basis of Lisiecki and Raymo data, was investigated by Dergachev and Dmitriev (2014) to reveal the hidden periodicities. The authors have found in this sample five periodicities of about 19, 22.4, 23.7, 41 and 98 kyrs which are similar to the Earth orbital cycles. It is clear that the climatic system does not respond linearly to the insolation variations though astronomical frequencies corresponding to orbital cycles are found in almost all paleoclimatic records. Ice cores from Greenland and Antarctica provide at present the most detailed information about climate change in the past. Figure 3 shows a comparison of changes in climate parameters in the ice core from the Antarctic Dome 2 station (concentration D) (Jouzel et al., 2007) and from ocean sediments (concentration 18 O) (Lisiecki and Raymo, 2005) during the last kyr. It is seen that the curves reflecting alteration of warm and cold periods nicely match each other. Over the last 800 kyr, the orbital cycles were the dominant causes and pace-makers for climate variability. Global temperatures cooled at irregular rates during the extended glacial epochs and rose much faster at the beginning of the interglacials (MIS-1 MIS-19). These interglacials recurred during the recorded period at intervals of roughly 100,000 years and had durations typically of about 12,000 years. Documenting natural interglacial climate variability in the past provides a deeper understanding of the physical climate responses to orbital forcing. Figure 3. Comparison between climate changes reconstructed from Antarctic ice cores for various glacial interglacial intervals ( D) (Jouzel et al., 2007) and δ 18 O in ocean sediment cores (Lisiecki and Raymo, 2005) during the last 900 kyr. Interglacials are indicated MIS (Marine Isotope Stage). MIS-1 is the current interglacial. Detailed records from ice cores show that three previous interglacials (Figure 3) differ from the fourth which, as well as Holocene, coincides with the period when orbital eccentricity approaches to the minimum of a 400-thousand-year orbital cycle. The duration of the interglacial which took place ~ 400 kyr ago, is estimated to be much longer, than of the subsequent interglacial. New data with the updated age models, have provided an expanded view on temperature patterns during interglacials since 800 kyr (e.g., Rohling et al., 2012). However, there is currently no consensus on whether the interglacial periods have changed their intensity after ~430 kyr. 247
4 Interglacials Interglacials can be defined as time intervals, during which the global climate was incompatible with the wide extent of glacier conditions. In the context of future global warming induced by human activities, it is essential to assess the role of natural climatic variations. Precise knowledge of the duration of past interglacial periods is fundamental to the understanding of the potential future evolution of the Holocene. Past interglacials are characterized by different combinations of orbital forcing, atmospheric composition and climate responses. Palaeorecords from ice, land and oceans extend over the last 800 kyr, revealing eight glacial-interglacial cycles, with a range of insolation and greenhouse gas influences. To understand better our current interglacial (the Holocene, MIS-1 [Marine Isotope Stage]) and its future, it is necessary to investigate the response of the climate system to the peaks of interglacials in the past. Yin and Beger (2010) used the Earth system model of intermediate complexity to assess the contributions of insolation and greenhouse-gas concentrations to the climate associated with the peaks of all the interglacials over the past 800,000 years. The effect of boreal winters and of the Southern Hemisphere, which is also warmer during austral winters, on the carbon cycle should be assessed when investigating the underlying causes of the higher CO 2 concentrations during the later interglacials. The interglacials are compared in terms of their forcings and responses of surface air temperature, vegetation and sea ice. The results show that the relative magnitude of the simulated interglacials is in reasonable agreement with proxy data. The interglacials (Figure 4) display a correspondingly large variety of intensity and duration, thus providing an opportunity for major insights into the mechanisms involved in the behaviour of interglacial climates. A comparison of the duration of these interglacials, however, is often difficult, as the definition of the interglacial depends on the archive that is considered. Therefore, to compare interglacial length and climate conditions from different archives, a consistent definition of the interglacial conditions is required. The phasing and strengths of the precessional parameter and obliquity varied over past interglacials, influencing their timing, duration, and intensity (Tzedakis et al., 2012; Yin and Berger, 2012). Figure 4. Marine δ 18 O (Lisiecki and Raymo, 2005), precession and obliquity around the past 10 interglacial peaks ((Laskar et al., 2004)). The black bars localize δ 18 O minima, precession minima and obliquity maxima. The dates of δ 18 O minima and corresponding MISs (Tzedakis et al., 2012) are indicated. 248
5 Lang, and Wolff (2011) have compiled the data from 37 glacial, terrestrial and marine archives to obtain a data set covering years and allowing to study the features of glacial and interglacial periods. The comparison of interglacials concentrates on the peaks immediately before and after the terminations; particularly strong and weak interglacials have been identified. This confirms the idea that strong interglacials are limited to the last 450 kyr, and that this is a globally robust pattern. Orbital parameters as an analogue for the future current interglacial duration In order to understand better our current interglacial and its future, it is necessary to investigate the response of the climate system to insolation at the peaks of the interglacials with similar latitudinal and seasonal distribution of the incoming solar radiation over the past 800,000 years, which can lead to the similar climate response to insolation in the Holocene. Figure 5 shows three astronomical analogs of our Holocene interglacial in the vicinity of MIS-1, MIS-11 and MIS-19 (red arrows). The previous (in respect to the current one) interglacial period is marked by the green curve. Figure 5. Comparison of the orbital parameters (a) and various interglacial intervals (b). The red arrows show the analogs of the future current duration (Yin and Berger, 2012) of the current interglacial (blue). The green curve shows the last interglacial. Figure 6 compares similar latitudinal and seasonal distribution of the incoming solar radiation (precession and obliquity) and marine δ 18 O, around the past 3 interglacial peaks (MIS-1, MIS-11, MIS-19). MIS-1, MIS-11 and MIS-19 show as well similar latitudinal and seasonal distributions of the incoming solar radiation, which lead to similar climate response to insolation, however, differences exist. Recent research has focused on MIS 11 as a possible analog for the current interglacial, but the estimated length of MIS-11 seems to vary from 20 to 33 kyrs. Besides of this, it has been shown that MIS-11 consists of at least two insolation peaks. At the same time, MIS19 exhibits a very similar insolation minimum in the Holocene as MIS11, but it lasts for only kyr, similar to the current interglacial. Berger and Yin (2014) have shown that the equivalent of CO2 concentration is basically the same for MIS-1 and MIS-19 but larger for MIS-11. The evidences from MIS19 help to confine the debates about the real length of the current interglacial. 249
6 Figure 6. Marine δ 18 O, precession and obliquity around the past 3 interglacial peaks (MIS-1, MIS-11, MIS- 19). The black bars localize δ 18 O minima, precession minima and obliquity maxima (see Figure 4). The dates of δ 18 O minima and corresponding MISs are indicated. Conclusion The most recent researches have focused on MIS 11 as a possible analog for the current interglacial. However, MIS 11 spans two precession cycles, when the Holocene contains one insolation peak so far. Besides, the warm period around 400 kyr ago remains a contradiction. MIS-19 appears to be the best analogue for MIS-1. MIS19 represent a very similar insolation minimum to the Holocene and MIS11, but lasted for only kyr. It is interesting that CO2 concentration at that time were approximately 240 ppm. Thus with respect to the Holocene, MIS19 may act as a good analogue for climatic change under natural conditions, i.e. CO 2 levels are not influenced by mankind. Assuming the Holocene followed the pattern seen during MIS19, we would have expected that the inception of the next glacial period will start soon, if it is not already underway. References Berger, A. and Q. Yin (2014), About past interglacials as analogues to the Holocene and Anthropocene. Geophysical Research Abstracts Vol. 16, EGU , Dergachev, V.A., P.B. Dmitriev (2014), The orbital cycles of climate variability during the last three million years. XVIII Russian annual international conference Solar and Sun-Earth physics-2014» (20-24 October 2014, St. Petersburg, Pulkovo Observatory RAS). Grinsted, A., J.C. Moore, and S. Jevrejeva (2004), Application of the cross wavelet transform and wavelet coherence to geophysical time series. Nonlin. Processes Geophys., 11, Jouzel, J., V. Masson-Delmotte, O. Cattani, et al. (2007), Orbital and millennial Antarctic climate variability over the past Years, Science, 2007, 317, Lang, N.and E. W. Wolff (2011), Interglacial and glacial variability from the last 800 ka in marine, ice and terrestrial archives. Clim. Past, 7, , doi: /cp Laskar, J., P. Robutel, F. Joutel, M. Gastineau, A. C. M. Correia, and B. Levrard (2004), A long-term numerical solution for the insolation quantities of the Earth. Astron. Astrophys., 428(1), , doi: / : Milankovitch, M. (1948), Ausbau und gegenwartiger Stand der astronomischen Theorie der erdgeschichtlichen Klimate, Experientia, 4(11), , doi: /bf Rohling, E.J., A. Sluijs, H.A. Dijkstra, P. Köhler, R.S.W. van de Wal, et al. (2012), Making sense of palaeoclimate sensitivity. Nature, 491, , doi: /nature
7 Russon, T., M. Elliot, A. Sadekov, G. Cabioch, T. Corrège and P. De Deckker (2011), The mid-pleistocene transition in the subtropical southwest Pacific. Paleoceanography, 26 (1), March Tzedakis P.C., J. E. T. Channell, D. A. Hodell, H. F. Kleiven and L. C. Skinner (2012), Determining the natural length of the current interglacial. Nature Geoscience: 8 January 2012, doi: /ngeo1358. Yin, Q. Z. and A. Berger (2010), Insolation and CO 2 contribution to the interglacial climate before and after the Mid-Brunhes Event. Nature Geoscience, 3, , doi: /ngeo771. Yin, Q. Z. and A. Berger (2012), Individual contribution of insolation and CO2 to the interglacial climates of the past 800,000 years. Clim. Dynam., 38 (3-4), Zachos, J., M. Pagani, L. Sloan, E. Thomas, and K. Billups (2001), Trends, rhythms, and aberrations in global climate 65 Ma to present. Science, 292, Zachos, J.C., G.R. Dickens, and R.E. Zeebe (2008), An early Cenozoic perspective on greenhouse warming and carbon-cycle dynamics. Nature, 451,
Speleothems and Climate Models
Earth and Life Institute Georges Lemaître Centre for Earth and Climate Research Université catholique de Louvain, Belgium Speleothems and Climate Models Qiuzhen YIN Summer School on Speleothem Science,
More informationlecture 12 Paleoclimate
lecture 12 Paleoclimate OVERVIEW OF EARTH S CLIMATIC HISTORY Geologic time scales http://www.snowballearth.org/index.html Features of the climate during the Cretaceous period the land-sea distribution
More informationRecent Developments in the Theory of Glacial Cycles
Recent Developments in the Theory of Richard McGehee Seminar on the Mathematics of Climate Change School of Mathematics October 6, 010 Hansen, et al, Target atmospheric CO: Where should humanity aim? Open
More information8. Climate changes Short-term regional variations
8. Climate changes 8.1. Short-term regional variations By short-term climate changes, we refer here to changes occurring over years to decades. Over this timescale, climate is influenced by interactions
More informationClimate and Environment
Climate and Environment Oxygen Isotope Fractionation and Measuring Ancient Temperatures Oxygen Isotope Ratio Cycles Oxygen isotope ratio cycles are cyclical variations in the ratio of the mass of oxygen
More informationThe ocean s overall role in climate
The ocean s overall role in climate - moderates climate in time (diurnally, annually) - redistributes heat spatially in the largescale ocean circulation - lower albedo (sea ice higher albedo) - dry atmosphere
More informationIMA. Celestial Influences on Glacial Cycles. Math and Climate Seminar
Math and Climate Seminar IMA Celestial Influences on Richard McGehee Joint MCRN/IMA Math and Climate Seminar Tuesdays 11:15 1:5 streaming video available at www.ima.umn.edu Seminar on the Mathematics of
More informationMilankovitch Cycles. Milankovitch Cycles. Milankovitch Cycles. Milankovitch Cycles. Milankovitch Cycles. Milankovitch Cycles.
Richard McGehee Temperatures in the Cenozoic ra Seminar on the Mathematics of Climate Change School of Mathematics March 4, 9 http://www.tqnyc.org/nyc5141/beginningpage.html Hansen, et al, 8, p. 7 Recent
More informationToday s Climate in Perspective: Hendrick Avercamp ( ) ~1608; Rijksmuseum, Amsterdam
Today s Climate in Perspective: Paleoclimate Evidence Hendrick Avercamp (1585-1634) ~1608; Rijksmuseum, Amsterdam Observations Instrumental surface temperature records? (Le Treut et al., 2007 IPCC AR4
More informationIntroduction to Climate Change
Ch 19 Climate Change Introduction to Climate Change Throughout time, the earth's climate has always been changing produced ice ages Hence, climate variations have been noted in the past what physical processes
More informationMath /29/2014. Richard McGehee, University of Minnesota 1. Math 5490 September 29, Glacial Cycles
Math 9 September 29, 21 Topics in Applied Mathematics: Introduction to the Mathematics of Climate Mondays and Wednesdays 2: : http://www.math.umn.edu/~mcgehee/teaching/math9-21-2fall/ Streaming video is
More informationAn Orbital Theory for Glacial Cycles
An Orbital Theory for Glacial Cycles Peter Bogenschutz March 2006 1. Introduction In the late 1800's, when ice ages were first discovered, variations in Earth's orbital mechanics were hypothesized to be
More informationToday we will discuss global climate: how it has changed in the past, and how the current status and possible future look.
Global Climate Change Today we will discuss global climate: how it has changed in the past, and how the current status and possible future look. If you live in an area such as the Mississippi delta (pictured)
More informationNatural Climate Variability: Longer Term
Natural Climate Variability: Longer Term Natural Climate Change Today: Natural Climate Change-2: Ice Ages, and Deep Time Geologic Time Scale background: Need a system for talking about unimaginable lengths
More informationPaleoclimate: What can the past tell us about the present and future? Global Warming Science February 14, 2012 David McGee
Paleoclimate: What can the past tell us about the present and future? 12.340 Global Warming Science February 14, 2012 David McGee 1 Recent observed trends: Greenhouse gases Image courtesy of NOAA. 2 Recent
More informationNATS 101 Section 13: Lecture 32. Paleoclimate
NATS 101 Section 13: Lecture 32 Paleoclimate Natural changes in the Earth s climate also occur at much longer timescales The study of prehistoric climates and their variability is called paleoclimate.
More informationGlacial-Interglacial Cycling: Ice, orbital theory, and climate. Dr. Tracy M. Quan IMCS
Glacial-Interglacial Cycling: Ice, orbital theory, and climate Dr. Tracy M. Quan IMCS quan@marine.rutgers.edu Outline -The past - discovery of glacial periods - introduction of orbital theory -The present
More informationUnderstanding past climate change
Steven J. Phipps ARC Centre of Excellence for Climate System Science Climate Change Research Centre University of New South Wales CLIM1001 Introduction to Climate Change 3 September 2013 1 Why past climates
More informationDevelopment of the Global Environment
Development of the Global Environment G302: Spring 2004 A course focused on exploration of changes in the Earth system through geological history Simon C. Brassell Geological Sciences simon@indiana.edu
More informationWelcome to ATMS 111 Global Warming.
Welcome to ATMS 111 Global Warming http://www.atmos.washington.edu/2010q1/111 Isotopic Evidence 16 O isotopes "light 18 O isotopes "heavy" Evaporation favors light Rain favors heavy Cloud above ice is
More informationPleistocene Glaciation (Ch.14) Geologic evidence Milankovitch cycles Glacial climate feedbacks
Pleistocene Glaciation (Ch.14) Geologic evidence Milankovitch cycles Glacial climate feedbacks End of last ice-age rise of human civilization Modern ice-ages begin Asteroid impact end of dinosaurs Cambrian
More informationOur Geologic Backdrop: Ice Age Cycles
Introduction to Earth s Climate System Our Geologic Backdrop: Ice Age Cycles MODULE 2.4 2.4 Our Geologic Backdrop: Ice Age Cycles Lesson Goals»» Describe Earth s geologic variability over the past million
More informationREVISITING THE ANALOGUE FOR THE COMING ICE AGE
REVISITING THE ANALOGUE FOR THE COMING ICE AGE When paleoclimatologists gathered in 1972 to discuss how and when the present warm climate would end, termination of this warm climate we call the Holocene
More informationIce Ages and Changes in Earth s Orbit. Topic Outline
Ice Ages and Changes in Earth s Orbit Topic Outline Introduction to the Quaternary Oxygen isotopes as an indicator of ice volume Temporal variations in ice volume Periodic changes in Earth s orbit Relationship
More informationTOPIC #12 NATURAL CLIMATIC FORCING
TOPIC #12 NATURAL CLIMATIC FORCING (Start on p 67 in Class Notes) p 67 ENERGY BALANCE (review) Global climate variability and change are caused by changes in the ENERGY BALANCE that are FORCED review FORCING
More informationIntroduction to Quaternary Geology (MA-Modul 3223) Prof. C. Breitkreuz, SS2012, TU Freiberg
Introduction to Quaternary Geology (MA-Modul 3223) Prof. C. Breitkreuz, SS2012, TU Freiberg 1. Introduction: - Relevance, and relations to other fields of geoscience - Lower stratigraphic boundary and
More informationPleistocene Glaciations
Chapter 14 Pleistocene Glaciations I. Geologic evidence 1. glacial deposits, etc. Pleistocene Glaciations 2. The Oxygen Isotope Record (1970s) II. Explanation of the glacial-interglacial periods The Milankovitch
More informationThe Ice Age sequence in the Quaternary
The Ice Age sequence in the Quaternary Subdivisions of the Quaternary Period System Series Stage Age (Ma) Holocene 0 0.0117 Tarantian (Upper) 0.0117 0.126 Quaternary Ionian (Middle) 0.126 0.781 Pleistocene
More informationHistory. Late 18 th /early 19 th century Europeans observed that erratic boulders dispersed due to the retention of glaciers caused by climate chance
Ice ages What is an ice age? Geological period of long-term reduction in the temperature of the Earth's surface and atmosphere which results in the formation and expansion of continental ice sheets, polar
More informationTOPIC #12. Wrap Up on GLOBAL CLIMATE PATTERNS
TOPIC #12 Wrap Up on GLOBAL CLIMATE PATTERNS POLE EQUATOR POLE Now lets look at a Pole to Pole Transect review ENERGY BALANCE & CLIMATE REGIONS (wrap up) Tropics Subtropics Subtropics Polar Extratropics
More informationMAR110 LECTURE #28 Climate Change I
25 November 2007 MAR 110 Lec28 Climate Change I 1 MAR110 LECTURE #28 Climate Change I Figure 28.1 Climate Change Diagnostics Drought and flooding represent just a couple of hazards related to climate variability
More informationENIGMA: something that is mysterious, puzzling, or difficult to understand.
Lecture 12. Attempts to solve the Eccentricity Enigma ENIGMA: something that is mysterious, puzzling, or difficult to understand. Milankovitch forcing glacier responses pre-900,000 yr BP glacier responses
More informationFather of Glacial theory. First investigations of glaciers and mountain geology,
First investigations of glaciers and mountain geology, 1750-1800 Glaciation happens! -- Historical perspective It happens in cycles -- How do we know this? What are Milankovitch cycles? Sub-Milankovitch
More informationThe Pleistocene Ice Ages
The Pleistocene Ice Ages 5 15 25 35 45 55 65 EPOCH QART PLIO CRETACEOUS PALEOCENE EOCENE OLIGOCENE MIOCENE Nalma * Irving./RLB Blancan Hemphillian Clarendonian Barstovian Hemingfordian Arikareean Whitneyan
More informationATMS 321: Natural Climate Variability Chapter 11
ATMS 321: Natural Climate Variability Chapter 11 Solar Variability: Total solar irradiance variability is relatively small about a tenth of a percent. Ultraviolet variability is larger, and so could affect
More informationSummary. The Ice Ages and Global Climate
The Ice Ages and Global Climate Summary Earth s climate system involves the atmosphere, hydrosphere, lithosphere, and biosphere. Changes affecting it operate on time scales ranging from decades to millions
More informationPaleoceanography II Telluric Effects on Oceanography
Paleoceanography II Telluric Effects on Oceanography Geological Oceanography OCN 622 Gary McMurtry Telluric Effects Tellus = Earth Distribution of Continents at 100 Ma BP and Present Comparison of Earth
More informationOrbital-Scale Interactions in the Climate System. Speaker:
Orbital-Scale Interactions in the Climate System Speaker: Introduction First, many orbital-scale response are examined.then return to the problem of interactions between atmospheric CO 2 and the ice sheets
More informationThe Distribution of Cold Environments
The Distribution of Cold Environments Over 25% of the surface of our planet can be said to have a cold environment, but defining what we actually mean by that can be very challenging. This is because cold
More information"Global Warming Beer" Taps Melted Arctic Ice (UPDATE)
"Global Warming Beer" Taps Melted Arctic Ice (UPDATE) The brewery filed for bankruptcy in Aug 2008 The Greenland Brewhouse is the world's first Inuit microbrewery. The water, the brewers say, is the beer's
More informationIce on Earth: An overview and examples on physical properties
Ice on Earth: An overview and examples on physical properties - Ice on Earth during the Pleistocene - Present-day polar and temperate ice masses - Transformation of snow to ice - Mass balance, ice deformation,
More informationChapter Causes of Climate Change Part I: Milankovitch Cycles
Chapter 19.1-19.3 Causes of Climate Change Part I: Milankovitch Cycles Climate Cycles =400 Milankovitch Cycles Milankovitch Cycles are created by changes in the geometry of Earth s orbit around the sun
More informationERS 121 Study Guide for Exam 1. Lecture 1. Ice Age Theory 1. Where did the ice age theory originate?
Lecture 1. Ice Age Theory 1. Where did the ice age theory originate? ERS 121 Study Guide for Exam 1 2. Where did J. P. Perraudin live? What did he suggest? 3. Who was Ignace Venetz? 4. Who was Jean de
More informationGlobal climate change
Global climate change What is climate change? This winter was really cold! Temp difference ( C): Jan 2004 vs. Jan 2002-2003 Make your own maps at: http://www.giss.nasa.gov/data/update/gistemp/maps/ 1 What
More information6. What has been the most effective erosive agent in the climate system? a. Water b. Ice c. Wind
Multiple Choice. 1. Heinrich Events a. Show increased abundance of warm-water species of planktic foraminifera b. Show greater intensity since the last deglaciation c. Show increased accumulation of ice-rafted
More informationA GCM Reconstruction of the Last Glacial Inception
A GCM Reconstruction of the Last Glacial Inception Megan Essig 1, Francis Otieno 2, Robert Oglesby 1, David Bromwich 2 1 Department of Geosciences, University of Nebraska, Lincoln 2 Polar Meteorology Group,
More informationClimate Changes: Past & Future (Ch 16) Iceberg 100km east of Dunedin, South Island, New Zealand, 2006
Climate Changes: Past & Future (Ch 16) Climate change change in any statistical property of earth-atmosphere climate system in response to alteration of an external boundary condition or as an internal
More informationChapter 15 Millennial Oscillations in Climate
Chapter 15 Millennial Oscillations in Climate This chapter includes millennial oscillations during glaciations, millennial oscillations during the last 8000 years, causes of millennial-scale oscillations,
More informationPaleoclimatology ATMS/ESS/OCEAN 589. Abrupt Climate Change During the Last Glacial Period
Paleoclimatology ATMS/ESS/OCEAN 589 Ice Age Cycles Are they fundamentaly about ice, about CO2, or both? Abrupt Climate Change During the Last Glacial Period Lessons for the future? The Holocene Early Holocene
More informationEnergy Balance Models
Richard McGehee School of Mathematics University of Minnesota NCAR - MSRI July, 2010 Earth s Energy Balance Gary Stix, Scientific American September 2006, pp.46-49 Earth s Energy Balance Historical Overview
More informationGlobal Paleogeography
Global Paleogeography Overview of Global Paleogeography Paleogeography is the study of how the Earth s geography has changed during the course of history. Using geological data, scientists reconstruct
More informationATOC OUR CHANGING ENVIRONMENT
ATOC 1060-002 OUR CHANGING ENVIRONMENT Class 22 (Chp 15, Chp 14 Pages 288-290) Objectives of Today s Class Chp 15 Global Warming, Part 1: Recent and Future Climate: Recent climate: The Holocene Climate
More informationChp Spectral analysis a. Requires that the climate record must be at least 4 times longer than the cycled analyzed
Chp 7 1. Earth s seasons are caused by a. The movement of the Sun from North to South of the equator and back again over a year s time b. The distance between Earth and the Sun c. The rate of Earth s movement
More informationMAR110 LECTURE #22 Climate Change
MAR 110: Lecture 22 Outline Climate Change 1 MAR110 LECTURE #22 Climate Change Climate Change Diagnostics Drought and flooding represent just a couple of hazards related to climate variability (O) The
More informationOutline 23: The Ice Ages-Cenozoic Climatic History
Outline 23: The Ice Ages-Cenozoic Climatic History Continental Glacier in Antarctica Valley Glaciers in Alaska, note the moraines Valley Glaciers in Alaska, note the moraines Mendenhall Glacier, Juneau,
More informationLecture 21: Glaciers and Paleoclimate Read: Chapter 15 Homework due Thursday Nov. 12. What we ll learn today:! Learning Objectives (LO)
Learning Objectives (LO) Lecture 21: Glaciers and Paleoclimate Read: Chapter 15 Homework due Thursday Nov. 12 What we ll learn today:! 1. 1. Glaciers and where they occur! 2. 2. Compare depositional and
More informationNatural and anthropogenic climate change Lessons from ice cores
Natural and anthropogenic climate change Lessons from ice cores Eric Wolff British Antarctic Survey, Cambridge ewwo@bas.ac.uk ASE Annual Conference 2011; ESTA/ESEU lecture Outline What is British Antarctic
More informationExtent of Periglacial = Global Permafrost Permafrost: Soil and/or rock where temperatures remain below 0 degrees C for 2 or more years.
Geog 1000 - Lecture 34 Periglacial Environments and Paleoclimatology http://scholar.ulethbridge.ca/chasmer/classes/ Today s Lecture (Pgs 422-434) 1. Exam questions from last week, and today 2. Extent of
More informationGlacial Cycles: from Aristotle to Hogg and Back to Budyko
Glacial Cycles: from Aristotle to Hogg and Back to Budyko Richard McGehee School of Mathematics University of Minnesota Climate Change Summer School Mathematical Sciences Research Institute July 28, 2008
More informationWhen Did the Anthropocene Begin? Observations and Climate Model Simulations
When Did the Anthropocene Begin? Observations and Climate Model Simulations by John Kutzbach University of Wisconsin-Madison March 31, 2011 Colleagues: W. Ruddiman, S. Vavrus, G. Philippon-Berrthier Main
More informationPaleoclimate indicators
Paleoclimate indicators Rock types as indicators of climate Accumulation of significant thicknesses of limestone and reef-bearing limestone is restricted to ~20º + - equator Gowganda tillite, Ontario
More informationMonday, December 4, 2017 The Pleistocene Glaciations (Chapter 14) Week 14 Assessment, closes Wednesday Dec 6
Monday, December 4, 2017 The Pleistocene Glaciations (Chapter 14) Week 14 Assessment, closes Wednesday Dec 6 Week 15 Assessment will be last one, closes Wednesday Dec 13 Homework 5 due Wednesday, Dec 6
More informationLessons from the past: interpreting the paleorecord & modelling
Agenda ATLAB WP5 Workshop - June 11-13, 2014 Lessons from the past: interpreting the paleorecord & modelling ING PAN, Research Centre in Kraków 1. DAY - Wednesday - 11.06.2014 General introduction into
More informationVariations in the Earth's Orbit: Pacemaker of the Ice Ages
Variations in the Earth's Orbit: Pacemaker of the Ice Ages For 500,000 years, major climatic changes have followed variations in obliquity and precession. J. D. Hays, John Imbrie, N. J. Shackleton Science,
More informationWe re living in the Ice Age!
Chapter 18. Coping with the Weather: Causes and Consequences of Naturally Induce Climate Change 지구시스템의이해 We re living in the Ice Age! 1 Phanerozoic Climate 서늘해지고 더웠고 따뜻했고 3 Climate Rollercoaster 4 2 Time
More informationComponents of the Climate System. Lecture 2: Earth s Climate System. Pop Quiz. Sub-components Global cycles What comes in What goes out
Lecture 2: Earth s Climate System Components of the Climate System terrestrial radiation Atmosphere Ocean solar radiation Land Energy, Water, and Biogeochemistry Cycles Sub-components Global cycles What
More informationLast Time. Submarine Canyons and Fans. Turbidites. MAS 603: Geological Oceanography. Lecture 16: Greenhouse vs. Icehouse Earths
UNIVERSITY OF SOUTH ALABAMA Last Time MAS 603: Geological Oceanography Lecture 16: Greenhouse vs. Icehouse Earths Submarine Fans Definition and morphology Transport mechanisms (density currents) Submarine
More informationLecture 2: Earth s Climate System
Lecture 2: Earth s Climate System terrestrial radiation solar radiation Atmosphere Ocean Solid Earth Land Energy, Water, and Biogeochemistry Cycles Sub-components Global cycles What comes in What goes
More informationCORRELATION OF CLIMATIC AND SOLAR VARIATIONS OVER THE PAST 500 YEARS AND PREDICTING GLOBAL CLIMATE CHANGES FROM RECURRING CLIMATE CYCLES
Easterbrook, D.J., 2008, Correlation of climatic and solar variations over the past 500 years and predicting global climate changes from recurring climate cycles: International Geological Congress, Oslo,
More informationRecent Climate History - The Instrumental Era.
2002 Recent Climate History - The Instrumental Era. Figure 1. Reconstructed surface temperature record. Strong warming in the first and late part of the century. El Ninos and major volcanic eruptions are
More informationEarly Earth. Geologic Time. Rise of Oxygen. Early Life. Scott Denning CSU Atmospheric Science 1
Geologic Time Precambrian, and then everything else! (It s always down there) Primary, Secondary, Tertiary Fossils told this story Early Earth Formed by accretion ~ 4.7 billion years ago Solar constant
More informationLecture 10: Seasons and Ice Age. Earth s Orbit and Its Variations. Perihelion and Aphelion. Tilt Produces Seasons
Lecture 10: Seasons and Ice Age Earth s Orbit and Its Variations! Earth s Orbit and Its Variations! How Seasons Are produced! Milankovitch Theory on Glacial-Interglacial Cycle (from The Earth System)!
More informationClimate Change. April 21, 2009
Climate Change Chapter 16 April 21, 2009 Reconstructing Past Climates Techniques Glacial landscapes (fossils) CLIMAP (ocean sediment) Ice cores (layering of precipitation) p Otoliths (CaCO 3 in fish sensory
More informationA GEOLOGICAL VIEW OF CLIMATE CHANGE AND GLOBAL WARMING
A GEOLOGICAL VIEW OF CLIMATE CHANGE AND GLOBAL WARMING Compiled by William D. Pollard, M Ray Thomasson PhD, and Lee Gerhard PhD THE ISSUE - Does the increase of carbon dioxide in the atmosphere, resulting
More informationThe North Atlantic Oscillation: Climatic Significance and Environmental Impact
1 The North Atlantic Oscillation: Climatic Significance and Environmental Impact James W. Hurrell National Center for Atmospheric Research Climate and Global Dynamics Division, Climate Analysis Section
More informationTropical Ocean Temperatures Over the Past 3.5 Million Years
www.sciencemag.org/cgi/content/full/328/5985/1530/dc1 Supporting Online Material for Tropical Ocean Temperatures Over the Past 3.5 Million Years Timothy D. Herbert, Laura Cleaveland Peterson, Kira T. Lawrence,
More informationEarth s narrow escape from a big freeze
RESEARCH NEWS & VIEWS CLIMATE SCIENCE Earth s narrow escape from a big freeze An equation has been derived that allows the timing of the onset of glaciations to be predicted. This confirms that Earth has
More informationChapter 6: Global Climate Change
Chapter 6: Global Climate Change Section 1: Paleoclimate The cross section of a tree trunk shows numerous rings. What do you think the light and dark rings represent? What can you infer about climate from
More informationEarth s Heat Budget. What causes the seasons? Seasons
Earth s Heat Budget Solar energy and the global heat budget Transfer of heat drives weather and climate Ocean circulation A. Rotation of the Earth B. Distance from the Sun C. Variations of Earth s orbit
More informationClimate Changes due to Natural Processes
Climate Changes due to Natural Processes 2.6.2a Summarize natural processes that can and have affected global climate (particularly El Niño/La Niña, volcanic eruptions, sunspots, shifts in Earth's orbit,
More informationMarine Oxygen Isotopes and Changes in Global Ice Volume
Marine Oxygen Isotopes and Changes in Global Ice Volume Name: You have learned about the value of marine oxygen-isotope records for understanding changes in ocean-water temperature and global ice volume
More informationAn Arctic Perspective on Climate Change
An Arctic Perspective on Climate Change 23 Oct 2012 Gifford Miller (and many others) University of Colorado Boulder The Earth is warming How do we know? Temperature Anomaly ( C) It s a fact Global Land
More informationGlobal Warming: The known, the unknown, and the unknowable
Global Warming: The known, the unknown, and the unknowable Barry A. Klinger Jagadish Shukla George Mason University (GMU) Institute of Global Environment and Society (IGES) January, 2008, George Mason
More informationQuarternary Climate Variations
Quarternary Climate Variations EAS 303 Lecture 34 Background and History Louis Agassiz (1840): recognition of Ice Ages Harold Urey (1947): The Thermodynamic Properties of Isotopic Substances calculated
More informationLecture 8. The Holocene and Recent Climate Change
Lecture 8 The Holocene and Recent Climate Change Recovery from the last ice age About 15,000 years ago, the earth began to warm and the huge ice sheets covering much of North America and Eurasia began
More informationAPPLICATION OF DYNAMIC PROGRAMMING TO THE DATING OF A LOESS-PALEOSOL SEQUENCE
Romanian Reports in Physics, Vol. 60, No. 1, P. 157 171, 2008 APPLICATION OF DYNAMIC PROGRAMMING TO THE DATING OF A LOESS-PALEOSOL SEQUENCE C. NECULA, C. PANAIOTU University of Bucharest, Faculty of Physics,
More informationTopic 6: Insolation and the Seasons
Topic 6: Insolation and the Seasons Solar Radiation and Insolation Insolation: In Sol ation The Sun is the primary source of energy for the earth. The rate at which energy is radiated is called Intensity
More information4 Changes in Climate. TAKE A LOOK 2. Explain Why is more land exposed during glacial periods than at other times?
Name Class CHAPTER 3 Date Climate 4 Changes in Climate SECTION National Science Education Standards BEFORE YOU READ After you read this section, you should be able to answer these questions: ES 1k, 2a
More informationHow long will the precession epoch last in terms of Pleistocene glacial cycles?
RUSSIAN JOURNAL OF EARTH SCIENCES, VOL. 10, ES3004, doi:10.2205/2008es000299, 2008 How long will the precession epoch last in terms of Pleistocene glacial cycles? V. A. Bol shakov 1 Received 6 March 2008;
More informationOutline 24: The Holocene Record
Outline 24: The Holocene Record Climate Change in the Late Cenozoic New York Harbor in an ice-free world (= Eocene sea level) Kenneth Miller, Rutgers University An Ice-Free World: eastern U.S. shoreline
More information2/18/2013 Estimating Climate Sensitivity From Past Climates Outline
Estimating Climate Sensitivity From Past Climates Outline Zero-dimensional model of climate system Climate sensitivity Climate feedbacks Forcings vs. feedbacks Paleocalibration vs. paleoclimate modeling
More informationProf. Dr. Anders Levermann Junior Professor for climate modelling on long timescales, Potsdam Institute for Climate Impact Research, Potsdam, Germany
Prof. Dr. Anders Levermann Junior Professor for climate modelling on long timescales, Potsdam Institute for Climate Impact Research, Potsdam, Germany Points for discussion: The state of global climate;
More informationOrbital- Scale Climate Changes. GEOG 401: Climatology Dr. John Abatzoglou
Orbital- Scale Climate Changes GEOG 401: Climatology Dr. John Abatzoglou Ice Core Sampling Typically performed at top of ice dome where less lateral spreading occurs Diffusion issue can make high- resoluion
More informationLecture 10. Orbital-scale changes in greenhouse gases Ruddiman Chapter 11
Lecture 10. Orbital-scale changes in greenhouse gases Ruddiman Chapter 11 The key questions: 1) Role of GHGs in ice ages? 2) Does Milankovitch explain the timing of the ice ages? Bill Ruddiman Main points:
More informationEvidence of Climate Change in Glacier Ice and Sea Ice
Evidence of Climate Change in Glacier Ice and Sea Ice John J. Kelley Institute of Marine Science School of Fisheries and Ocean Sciences University of Alaska Fairbanks Evidence for warming of the Arctic
More informationIn the summer of 1836, Agassiz stayed with a well known geologist (Chapentier) who had been convinced by a collegue (Venetz) of extensive Alpine
4 Cilvilization exists by geological consent, subject to change without notice, Will Durant. In 1807 the Geological Society of London had concerns that too many people would join: it was the sexy science
More informationChapter Introduction. Earth. Change. Chapter Wrap-Up
Chapter Introduction Lesson 1 Lesson 2 Lesson 3 Climates of Earth Chapter Wrap-Up Climate Cycles Recent Climate Change What is climate and how does it impact life on Earth? What do you think? Before you
More information( 1 d 2 ) (Inverse Square law);
ATMO 336 -- Exam 3 120 total points including take-home essay Name The following equations and relationships may prove useful. F d1 =F d2 d 2 2 ( 1 d 2 ) (Inverse Square law);! MAX = 0.29 " 104 µmk (Wien's
More informationClimate Change 2007: The Physical Science Basis
Climate Change 2007: The Physical Science Basis Working Group I Contribution to the IPCC Fourth Assessment Report Presented by R.K. Pachauri, IPCC Chair and Bubu Jallow, WG 1 Vice Chair Nairobi, 6 February
More informationAgronomy 406 World Climates
Agronomy 406 World Climates April 3, 2018 Causes of natural climate changes (finish). Schedule is being adjusted. No change to due dates. Bring IPCC Fifth Assessment Report Summary for Policymakers to
More information