With the exception of Chapter and Section headings, all coloured text has been inserted by AccessIPCC. The non-coloured text is the IPCC original.

A number of emails from the Climate Research Unit (CRU) of the University of East Anglia were published on the Internet in November 2009. This has provided a window into the world of climate science.

We have identified a number of key individuals involved in the emails whom we have designated as Persons of Concern [PoC]; a Journal in which a PoC has published has been designated as a Journal of Concern [JoC].

This is not to suggest that we believe such papers are necessarily flawed, but rather that, as Joseph Alcamo noted at Bali in October 2009, "as policymakers and the public begin to grasp the multi-billion dollar price tag for mitigating and adapting to climate change, we should expect a sharper questioning of the science behind climate policy".

References occur in a list at the end of each chapter. Citations are within the normal text of sections and paragraphs.

Definition of Tags Used

Tag	Explanation	Where Used	References	Citations
PoC	Person of Concern Key individual involved in CRU emails as defined in this spreadsheet. NOTE: we anticipate that this definition will be expanded as more data is coded.	References, Citations, IPCC Roles	85	163
JoC	Journal of Concern A Journal which has published articles by one or more PoCs (Person of Concern)	References, Citations	454	699
MoS	Model or Simulation Reference appears to be a model or simulation, not observation or experiment	References, Citations	130	200
NPR	Non Peer Reviewed Reference has no Journal or no Volume or no Pages or it has Editors.	References, Citations	62	82
SRC	Self Reference Concern Author of a chapter containing references to own work.	References, Citations, IPCC Roles	116	199
ARC	Paper authored or co-authored by person who is also in list of Authors of another chapter.	References, Citations	110	151
2007	Paper dated 2007, when IPCC policy stated cutoff was December 2005 with mid-February 2006 for exceptions.	References, Citations	3	4
Ambiguous	The short inline citation matched with more than one reference; however, AccessIPCC will link to the first reference found.	Citations	-	8
NotFound	The short inline citation was not matched with any reference. Believed to be caused by typing errors.	Citations	-	8
Clean	The reference was probably peer reviewed. The reference was dated before the cutoff (2005-2006). Its authors were not members of the Team. It was not published in a Journal of Concern. Its authors were not AR4 Authors.	References, Citations	76	103

Chapter Table of Contents

Title	Clean	Tagged	NotFound	Ambiguous
Chapter 6: Palaeoclimate	-	-	-	-
6.1 Introduction	-	4	-	-
6.2 Palaeoclimatic Methods	-	-	-	-
6.2.1 Methods – Observations of Forcing and Response	-	8	-	-
6.2.1.1 How are Past Climate Forcings Known?	-	-	-	-
6.2.1.2 How are Past Changes in Global Atmospheric Composition Known?	-	-	-	-
6.2.1.3 How Precisely Can Palaeoclimatic Records of Forcing and Response be Dated?	-	-	-	-
6.2.1.4 How Can Palaeoclimatic Proxy Methods Be Used to Reconstruct Past Climate Dynamics?	-	-	-	-
6.2.2 Methods – Palaeoclimate Modelling	-	1	-	-
6.3 The Pre-Quaternary Climates	-	-	-	-
6.3.1 What is the Relationship Between Carbon Dioxide and Temperature in this Time Period?	6	21	-	-
6.3.2 What Does the Record of the Mid-Pliocene Show?	5	24	-	-
6.3.3 What Does the Record of the Palaeocene-Eocene Thermal Maximum Show?	2	20	-	-
6.4 Glacial-Interglacial Variability and Dynamics	-	-	-	-
6.4.1 Climate Forcings and Responses Over Glacial-Interglacial Cycles	2	35	-	-
6.4.1.1 How Do Glacial-Interglacial Variations in the Greenhouse Gases Carbon Dioxide, Methane and Nitrous Oxide Compare with the Industrial Era Greenhouse Gas Increase?	-	34	-	-
6.4.1.2 What Do the Last Glacial Maximum and the Last Deglaciation Show?	7	32	-	-
6.4.1.3 How Realistic Are Results from Climate Model Simulations of the Last Glacial Maximum?	1	21	1	-
6.4.1.4 How Realistic Are Simulations of Terrestrial Carbon Storage at the Last Glacial Maximum?	2	12	-	-
6.4.1.5 How Long Did the Previous Interglacials Last?	-	1	-	-
6.4.1.6 How Much Did the Earth Warm During the Previous Interglacial?	4	16	1	-
6.4.1.7 What Is Known About the Mechanisms of Transitions Into Ice Ages?	5	21	-	-
6.4.1.8 When Will the Current Interglacial End?	-	-	-	-
6.4.2 Abrupt Climatic Changes in the Glacial-Interglacial Record	-	-	-	-
6.4.2.1 What Is the Evidence for Past Abrupt Climate Changes?	8	33	-	-
6.4.2.2 What Is Known About the Mechanism of these Abrupt Changes?	1	21	-	-
6.4.2.3 Can Climate Models Simulate these Abrupt Changes?	-	19	-	-
6.4.3 Sea Level Variations Over the Last Glacial-Interglacial Cycle	-	-	-	-
6.4.3.1 What Is the Influence of Past Ice Volume Change on Modern Sea Level Change?	-	4	-	-
6.4.3.2 What Was the Magnitude of Glacial-Interglacial Sea Level Change?	-	14	-	-
6.4.3.3 What Is the Significance of Higher than Present Sea Levels During the Last Interglacial Period?	2	17	2	-
6.4.3.4 What Is the Long-Term Contribution of Polar Ice-sheet Derived Melt Water to the Observed Globally Averaged Rate of Sea Level Rise?	-	3	-	-
6.5 The Current Interglacial	-	-	-	-
6.5.1 Climate Forcing and Response During the Current Interglacial	-	-	-	-
6.5.1.1 What Were the Main Climate Forcings During the Holocene?	-	8	1	-
6.5.1.2 Why Did Holocene Atmospheric Greenhouse Gas Concentrations Vary Before the Industrial Period?	-	15	-	-
6.5.1.3 Was Any Part of the Current Interglacial Period Warmer than the Late 20th Century?	21	45	1	-
6.5.1.4 What Are the Links Between Orbital Forcing and Mid-Holocene Monsoon Intensification?	2	22	-	-
6.5.1.5 What Are the Links Between Orbital Forcing and mid-Holocene Climate at Middle and High Latitudes?	-	-	-	-
6.5.1.6 Are There Long-Term Modes of Climate Variability Identified During the Holocene that Could Be Involved in the Observed Current Warming?	4	21	-	-
6.5.2 Abrupt Climate Change During the Current Interglacial	-	-	-	-
6.5.2.1 What Do Abrupt Changes in Oceanic and Atmospheric Circulation at Mid- and High-Latitudes Show?	1	21	-	-
6.5.2.2 What Is the Understanding of Abrupt Changes in Monsoons?	1	4	-	1
6.5.3 How and Why Has the El Niño-Southern Oscillation Changed Over the Present Interglacial?	-	19	-	-
6.6 The Last 2,000 Years	-	-	-	-
6.6.1 Northern Hemisphere Temperature Variability	-	-	-	-
6.6.1.1 What Do Reconstructions Based on Palaeoclimatic Proxies Show?	8	124	-	4
6.6.1.2 What Do Large-Scale Temperature Histories from Subsurface Temperature Measurements Show?	3	25	-	-
6.6.2 Southern Hemisphere Temperature Variability	-	13	-	-
6.6.3 Comparisons of Millennial Simulations with Palaeodata	-	12	-	-
6.6.3.1 Solar Forcing	2	20	2	-
6.6.3.2 Volcanic Forcing	4	9	-	-
6.6.3.3 Industrial Era Sulphate Aerosols	3	1	-	-
6.6.3.4 Comparing Simulations of Northern Hemisphere Mean Temperatures with Palaeoclimatic Observations	-	18	-	2
6.6.4 Consistency Between Temperature, Greenhouse Gas and Forcing Records; and Compatibility of Coupled Carbon Cycle-Climate Models with the Proxy Records	-	6	-	-
6.6.5 Regional Variability in Quantities Other than Temperature	-	-	-	-
6.6.5.1 Changes in the El Niño-Southern Oscillation System	1	20	-	-
6.6.5.2 The Record of Past Atlantic Variability	-	14	-	1
6.6.5.3 Asian Monsoon Variability	8	4	-	-
6.6.5.4 Northern and Eastern Africa Hydrologic Variability	-	-	-	-
6.6.5.5 The Record of Hydrologic Variability and Change in the Americas	-	19	-	-
6.7 Concluding Remarks on Key Uncertainties	-	-	-	-
Number of citations of various credibilities	103	801	8	8
Percentages of citations of various credibilities	11.2%	87.1%	0.9%	0.9%

Executive Summary

What is the relationship between past greenhouse gas concentrations and climate?

• The sustained rate of increase over the past century in the combined radiative forcing from the three well-mixed greenhouse gases carbon dioxide (CO₂), methane (CH₄), and nitrous oxide (N₂O) is very likely unprecedented in at least the past 16 kyr. Pre-industrial variations of atmospheric greenhouse gas concentrations observed during the last 10 kyr were small compared to industrial era greenhouse gas increases, and were likely mostly due to natural processes.
• It is very likely that the current atmospheric concentrations of CO₂ (379 ppm) and CH₄ (1,774 ppb) exceed by far the natural range of the last 650 kyr. Ice core data indicate that CO₂ varied within a range of 180 to 300 ppm and CH₄ within 320 to 790 ppb over this period. Over the same period, antarctic temperature and CO₂ concentrations co-vary, indicating a close relationship between climate and the carbon cycle.
• It is very likely that glacial-interglacial CO₂ variations have strongly amplified climate variations, but it is unlikely that CO₂ variations have triggered the end of glacial periods. Antarctic temperature started to rise several centuries before atmospheric CO₂ during past glacial terminations.
• It is likely that earlier periods with higher than present atmospheric CO₂ concentrations were warmer than present. This is the case both for climate states over millions of years (e.g., in the Pliocene, about 5 to 3 Ma) and for warm events lasting a few hundred thousand years (i.e., the Palaeocene-Eocene Thermal Maximum, 55 Ma). In each of these two cases, warming was likely strongly amplified at high northern latitudes relative to lower latitudes.

What is the significance of glacial-interglacial climate variability?

• Climate models indicate that the Last Glacial Maximum (about 21 ka) was 3°C to 5°C cooler than the present due to changes in greenhouse gas forcing and ice sheet conditions. Including the effects of atmospheric dust content and vegetation changes gives an additional 1°C to 2°C global cooling, although scientific understanding of these effects is very low. It is very likely that the global warming of 4°C to 7°C since the Last Glacial Maximum occurred at an average rate about 10 times slower than the warming of the 20th century.
• For the Last Glacial Maximum, proxy records for the ocean indicate cooling of tropical sea surface temperatures (average likely between 2°C and 3°C) and much greater cooling and expanded sea ice over the high-latitude oceans. Climate models are able to simulate the magnitude of these latitudinal ocean changes in response to the estimated Earth orbital, greenhouse gas and land surface changes for this period, and thus indicate that they adequately represent many of the major processes that determine this past climate state.
• Last Glacial Maximum land data indicate significant cooling in the tropics (up to 5°C) and greater magnitudes at high latitudes. Climate models vary in their capability to simulate these responses.
• It is virtually certain that global temperatures during coming centuries will not be significantly influenced by a natural orbitally induced cooling. It is very unlikely that the Earth would naturally enter another ice age for at least 30 kyr.
• During the last glacial period, abrupt regional warmings (likely up to 16°C within decades over Greenland) and coolings occurred repeatedly over the North Atlantic region. They likely had global linkages, such as with major shifts in tropical rainfall patterns. It is unlikely that these events were associated with large changes in global mean surface temperature, but instead likely involved a redistribution of heat within the climate system associated with changes in the Atlantic Ocean circulation.
• Global sea level was likely between 4 and 6 m higher during the last interglacial period, about 125 ka, than in the 20th century. In agreement with palaeoclimatic evidence, climate models simulate arctic summer warming of up to 5°C during the last interglacial. The inferred warming was largest over Eurasia and northern Greenland, whereas the summit of Greenland was simulated to be 2°C to 5°C higher than present. This is consistent with ice sheet modelling suggestions that large-scale retreat of the south Greenland Ice Sheet and other arctic ice fields likely contributed a maximum of 2 to 4 m of sea level rise during the last interglacial, with most of any remainder likely coming from the Antarctic Ice Sheet.

What does the study of the current interglacial climate show?

• Centennial-resolution palaeoclimatic records provide evidence for regional and transient pre-industrial warm periods over the last 10 kyr, but it is unlikely that any of these commonly cited periods were globally synchronous. Similarly, although individual decadal-resolution interglacial palaeoclimatic records support the existence of regional quasi-periodic climate variability, it is unlikely that any of these regional signals were coherent at the global scale, or are capable of explaining the majority of global warming of the last 100 years.
• Glaciers in several mountain regions of the Northern Hemisphere retreated in response to orbitally forced regional warmth between 11 and 5 ka, and were smaller (or even absent) at times prior to 5 ka than at the end of the 20th century. The present day near-global retreat of mountain glaciers cannot be attributed to the same natural causes, because the decrease of summer insolation during the past few millennia in the Northern Hemisphere should be favourable to the growth of the glaciers.
• For the mid-Holocene (about 6 ka), GCMs are able to simulate many of the robust qualitative large-scale features of observed climate change, including mid-latitude warming with little change in global mean temperature (<0.4°C), as well as altered monsoons, consistent with the understanding of orbital forcing. For the few well-documented areas, models tend to underestimate hydrological change. Coupled climate models perform generally better than atmosphere-only models, and reveal the amplifying roles of ocean and land surface feedbacks in climate change.
• Climate and vegetation models simulate past northward shifts of the boreal treeline under warming conditions. Palaeoclimatic results also indicated that these treeline shifts likely result in significant positive climate feedback. Such models are also capable of simulating changes in the vegetation structure and terrestrial carbon storage in association with large changes in climate boundary conditions and forcings (i.e., ice sheets, orbital variations).
• Palaeoclimatic observations indicate that abrupt decadal- to centennial-scale changes in the regional frequency of tropical cyclones, floods, decadal droughts and the intensity of the African-Asian summer monsoon very likely occurred during the past 10 kyr. However, the mechanisms behind these abrupt shifts are not well understood, nor have they been thoroughly investigated using current climate models.

How does the 20th-century climate change compare with the climate of the past 2,000 years?

• It is very likely that the average rates of increase in CO₂,as well as in the combined radiative forcing from CO₂,CH₄ andN₂Oconcentration increases, have been at least five times faster over the period from 1960 to 1999 than over any other 40-year period during the past two millennia prior to the industrial era.
• Ice core data from Greenland and Northern Hemisphere mid-latitudes show a very likely rapid post-industrial era increase in sulphate concentrations above the pre-industrial background.
• Some of the studies conducted since the Third Assessment Report (TAR) indicate greater multi-centennial Northern Hemisphere temperature variability over the last 1 kyr than was shown in the TAR, demonstrating a sensitivity to the particular proxies used, and the specific statistical methods of processing and/or scaling them to represent past temperatures. The additional variability shown in some new studies implies mainly cooler temperatures (predominantly in the 12th to 14th, 17th and 19th centuries), and only one new reconstruction suggests slightly warmer conditions (in the 11th century, but well within the uncertainty range indicated in the TAR).
• The TAR pointed to the ‘exceptional warmth of the late 20th century, relative to the past 1,000 years’. Subsequent evidence has strengthened this conclusion. It is very likely that average Northern Hemisphere temperatures during the second half of the 20th century were higher than for any other 50-year period in the last 500 years. It is also likely that this 50-year period was the warmest Northern Hemisphere period in the last 1.3 kyr, and that this warmth was more widespread than during any other 50-year period in the last 1.3 kyr. These conclusions are most robust for summer in extratropical land areas, and for more recent periods because of poor early data coverage.
• The small variations in pre-industrial CO₂ and CH₄ concentrations over the past millennium are consistent with millennial-length proxy Northern Hemisphere temperature reconstructions; climate variations larger than indicated by the reconstructions would likely yield larger concentration changes. The small pre-industrial greenhouse gas variations also provide indirect evidence for a limited range of decadal- to centennial-scale variations in global temperature.
• Palaeoclimate model simulations are broadly consistent with the reconstructed NH temperatures over the past 1 kyr. The rise in surface temperatures since 1950 very likely cannot be reproduced without including anthropogenic greenhouse gases in the model forcings, and it is very unlikely that this warming was merely a recovery from a pre-20th century cold period.
• Knowledge of climate variability over the last 1 kyr in the Southern Hemisphere and tropics is very limited by the low density of palaeoclimatic records.
• Climate reconstructions over the past millennium indicate with high confidence more varied spatial climate teleconnections related to the El Niño-Southern Oscillation than are represented in the instrumental record of the 20th century.
• The palaeoclimate records of northern and eastern Africa, as well as the Americas, indicate with high confidence that droughts lasting decades or longer were a recurrent feature of climate in these regions over the last 2 kyr.

What does the palaeoclimatic record reveal about feedback, biogeochemical and biogeophysical processes?

• The widely accepted orbital theory suggests that glacial-interglacial cycles occurred in response to orbital forcing. The large response of the climate system implies a strong positive amplification of this forcing. This amplification has very likely been influenced mainly by changes in greenhouse gas concentrations and ice sheet growth and decay, but also by ocean circulation and sea ice changes, biophysical feedbacks and aerosol (dust) loading.
• It is virtually certain that millennial-scale changes in atmospheric CO₂ associated with individual antarctic warm events were less than 25 ppm during the last glacial period. This suggests that the associated changes in North Atlantic Deep Water formation and in the large-scale deposition of wind-borne iron in the Southern Ocean had limited impact on CO₂.
• It is very likely that marine carbon cycle processes were primarily responsible for the glacial-interglacial CO₂ variations. The quantification of individual marine processes remains a difficult problem.
• Palaeoenvironmental data indicate that regional vegetation composition and structure are very likely sensitive to climate change, and in some cases can respond to climate change within decades.

6.1 Introduction

This chapter assesses palaeoclimatic data and knowledge of how the climate system changes over interannual to millennial time scales, and how well these variations can be simulated with climate models. Additional palaeoclimatic perspectives are included in other chapters.

Palaeoclimate science has made significant advances since the 1970 s, when a primary focus was on the origin of the ice ages, the possibility of an imminent future ice age, and the first explorations of the so-called Little Ice Age and Medieval Warm Period. Even in the first IPCC assessment ( IPCC, 1990 [NPR] ), many climatic variations prior to the instrumental record were not that well known or understood. Fifteen years later, understanding is much improved, more quantitative and better integrated with respect to observations and modelling.

After a brief overview of palaeoclimatic methods, including their strengths and weaknesses, this chapter examines the palaeoclimatic record in chronological order, from oldest to youngest. This approach was selected because the climate system varies and changes over all time scales, and it is instructive to understand the contributions that lower-frequency patterns of climate change might make in influencing higher-frequency patterns of variability and change. In addition, an examination of how the climate system has responded to large changes in climate forcing in the past is useful in assessing how the same climate system might respond to the large anticipated forcing changes in the future.

Cutting across this chronologically based presentation are assessments of climate forcing and response, and of the ability of state-of-the-art climate models to simulate the responses. Perspectives from palaeoclimatic observations, theory and modelling are integrated wherever possible to reduce uncertainty in the assessment. Several sections also assess the latest developments in the rapidly advancing area of abrupt climate change, that is, forced or unforced climatic change that involves crossing a threshold to a new climate regime (e.g., new mean state or character of variability), often where the transition time to the new regime is short relative to the duration of the regime ( Rahmstorf, 2001 [NPR, PoC, SRC] ; Alley et al., 2003 [JoC, ARC] ; Overpeck and Trenberth, 2004 [NPR, PoC, MoS, SRC] ).

6.2 Palaeoclimatic Methods

6.3 The Pre-Quaternary Climates

6.4 Glacial-Interglacial Variability and Dynamics

6.5 The Current Interglacial

Avariety of proxy records provide detailed temporal and spatial information concerning climate change during the current interglacial, the Holocene, an approximately 11.6 kyr period of increasingly intense anthropogenic modifications of the local (e.g., land use) to global (e.g., atmospheric composition) environment. The well-dated reconstructions of the past 2 kyr are covered in Section 6.6 .In the context of both climate forcing and response, the Holocene is far better documented in terms of spatial coverage, dating and temporal resolution than previous interglacials. The evidence is clear that significant changes in climate forcing during the Holocene induced significant and complex climate responses, including long-term and abrupt changes in temperature, precipitation, monsoon dynamics and the El Niño-Southern Oscillation (ENSO). For selected periods such as the mid-Holocene, about 6 ka, intensive efforts have been dedicated to the synthesis of palaeoclimatic observations and modelling intercomparisons. Such extensive data coverage provides a sound basis to evaluate the capacity of climate models to capture the response of the climate system to the orbital forcing.

6.6 The Last 2,000 Years

6.7 Concluding Remarks on Key Uncertainties

Each palaeoclimatic time scale covered in this chapter contributes to the understanding of how the climate system varies naturally and also responds to changes in climate forcing. The existing body of knowledge is sufficient to support the assertions of this chapter. At the same time, key uncertainties remain, and greater confidence would result if these uncertainties were reduced.

Even though a great deal is known about glacial-interglacial variations in climate and greenhouse gases, a comprehensive mechanistic explanation of these variations remains to be articulated. Similarly, the mechanisms of abrupt climate change (for example, in ocean circulation and drought frequency) are not well enough understood, nor are the key climate thresholds that, when crossed, could trigger an acceleration in sea level rise or regional climate change. Furthermore, the ability of climate models to simulate realistic abrupt change in ocean circulation, drought frequency, flood frequency, ENSO behaviour and monsoon strength is uncertain. Neither the rates nor the processes by which ice sheets grew and disintegrated in the past are known well enough.

Knowledge of climate variability over the last 1 to 2 kyr in the SH and tropics is severely limited by the lack of palaeoclimatic records. In the NH, the situation is better, but there are important limitations due to a lack of tropical records and ocean records. Differing amplitudes and variability observed in available millennial-length NH temperature reconstructions, and the extent to which these differences relate to choice of proxy data and statistical calibration methods, need to be reconciled. Similarly, the understanding of how climatic extremes (i.e., in temperature and hydro-climatic variables) varied in the past is incomplete. Lastly, this assessment would be improved with extensive networks of proxy data that run right up to the present day. This would help measure how the proxies responded to the rapid global warming observed in the last 20 years, and it would also improve the ability to investigate the extent to which other, non-temperature, environmental changes may have biased the climate response of proxies in recent decades.

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NOTE: In the Summary of Reviewer Comments,
Accepted includes only those responses that were unambiguously Accepted.
There are other categories of responses that we have not yet quantified
due to inconsistencies of usage.

Summary of Reviewer Comments - Second Order Draft

Reviewer	Total Comments	Accepted	IPCC Roles	Papers
Gray, Vincent	131	8	0	0
Crucifix, M	119	42	0	8
Mcintyre, Stephen	108	18	0	0
Govt. of United States of America	99	31	0	0
Wolff, Eric	59	41	0	0
Govt. of Spain	53	27	0	0
Siddall, M	44	17	0	1
Mann, ME	37	8	0	23
Govt. of Australia	36	13	0	0
Crampton, James	34	17	0	0
Schulz, M	33	23	2	7
Wiles, G	30	9	1	0
Steig, Eric	26	9	0	0
Loutre, MF	26	14	2	11
Braconnot, P	21	12	1	7
Marquis, Melinda	20	8	0	0
Govt. of Germany	18	8	0	0
Crowley, TJ	17	6	0	11
Bauer, E	16	5	1	2
Waelbroeck, C	15	4	1	3
Mckitrick, Ross	14	5	0	0
Beltrami, H	13	4	0	4
Knutti, R	13	7	5	9
Muscheler, R	11	8	1	2
Stouffer, RJ	11	1	5	32
Harvey, D	10	3	1	1
Fahey, Dw&D	10	7	0	0
Alley, Rb	10	2	0	0
Simmons, AJ	10	4	1	3
Barrett, Peter	10	0	0	0
Schmidt, GA	9	6	1	14
Gerhard, Lee	9	1	0	0
Forster, PMF	8	8	7	7
Williams, Pw	8	0	0	0
Gonzalez-Rouco, Jf	8	4	0	0
Anderson, Wilmer	7	6	0	0
Nesje, A	7	5	0	7
Spahni, R	7	5	1	2
Kueter, Jeff	6	1	0	0
Calvo, Eva	6	2	0	0
Khodri, M	6	2	1	2
Woodhouse, Connie	6	0	0	0
Govt. of Sweden	6	1	0	0
Govt. of France	6	4	0	0
Tsu, Wg1	5	3	0	0
Jones, Gs	5	3	0	0
Matsumoto, K	4	0	1	1
Govt. of Thailand	4	2	0	0
Smith, SJ	4	2	1	2
Yokoyama, Y	4	0	0	1
Luterbacher, J	4	1	1	6
Govt. of China	4	1	0	0
Guiot, J	4	0	0	2
D'Arrigo, RD	4	2	0	8
Bernstein, Lenny	4	1	0	0
Zorita, E	3	0	1	8
Lacis, AA	3	2	0	3
Enting, Ian	3	3	0	0
Maccracken, Michael	3	0	0	0
Hu, AX	2	0	1	3
Holmund, Per	2	0	0	0
Hunter, John	2	0	0	0
Martin-Vide, Javier	2	2	0	0
Kandel, Robert	1	1	0	0
Michaels, Patrick	1	0	0	0
Muller, R	1	0	0	2
Marsh, RJ	1	0	1	5
Colombo, Tiziano	1	0	0	0
Soulen, Richard	1	0	0	0
Govt. of Japan	1	0	0	0
Su, Jilan	1	0	0	0
Roberts, Cn	1	0	0	0
Govt. of United Kingdom	1	1	0	0
Haeberli, W	1	0	0	2
Averyt, Kb	1	0	0	0
Totals	1231	430	37	199

Overview of Reviewer Comments - Second Order Draft

Reviewer Type	Total Comments	Accepted	% Accepted
Govt	228	88	38%
IPCC	498	200	40%
Indep	505	142	28%
Total	1231	430	34%

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