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1. Historical reconstruction of Plutonium contamination in the Swiss-Italian Alps

Author

Gabrieli J., Cozzi G., Vallelonga P., Schwikowski M., Sigl M., Boutron C., and Barbante C.

Subjects
Plutonium, Alps, ice, snow, ICP-SFMS, nuclear tests, Environmental sciences, GE1-350
Abstract

Plutonium is present in the environment as a consequence of atmospheric nuclear tests carried out in the 1960s, nuclear weapons production and releases by the nuclear industry over the past 50 years. Approximately 6 tons of 239Pu have been released into the environment as a result of 541 atmospheric weapon tests Nuclear Pu fallout has been studied in various environmental archives, such as sediments, soil and herbarium grass. Mid-latitude ice cores have been studied as well, on Mont Blanc, the Western Alps and on Belukha Glacier, Siberian Altai. We present a Pu record obtained by analyzing 52 discrete samples of an alpine firn/ice core from Colle Gnifetti (M. Rosa, 4450 m a.s.l.), dating from 1945 to 1991. The 239Pu signal was recorded directly, without preliminary cleaning or preconcentration steps, using an high resolution inductively plasma mass spectrometer equipped with a desolvation system. The 239Pu profile reflects the three main periods of atmospheric nuclear weapons testing: the earliest peak lasted from 1954/55 to 1958 and was caused by the first testing period reaching a maximum in 1958. Despite a temporary halt of testing in 1959/60, the Pu concentration decreased only by half with respect to the 1958 peak due to long atmospheric residence times. In 1961/62 Pu concentrations rapidly increased reaching a maximum in 1963. After the signing of the “Limited Test Ban Treaty” between USA and USSR in 1964, Pu deposition decreased very sharply reaching a minimum in 1967. The third period (1967-1975) is characterized by irregular Pu concentrations with smaller peaks which might be related to the deposition of Saharan dust contaminated by the French nuclear tests of the 1960s.

Published
2013
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2. The SP19 chronology for the South Pole Ice Core - Part 1: Volcanic matching and annual layer counting

Author

Winski, DA, Fudge, TJ, Ferris, DG, Osterberg, EC, Fegyveresi, JM, Cole-Dai, J, Thundercloud, Z, Cox, TS, Kreutz, KJ, Ortman, N, Buizert, C, Epifanio, J, Brook, EJ, Beaudette, R, Severinghaus, J, Sowers, T, Steig, EJ, Kahle, EC, Jones, TR, Morris, V, Aydin, M, Nicewonger, MR, Casey, KA, Alley, RB, Waddington, ED, Iverson, NA, Dunbar, NW, Bay, RC, Souney, JM, Sigl, M, and McConnell, JR

Subjects
Paleontology, Physical Geography and Environmental Geoscience
Abstract

The South Pole Ice Core (SPICEcore) was drilled in 2014-2016 to provide a detailed multi-proxy archive of paleoclimate conditions in East Antarctica during the Holocene and late Pleistocene. Interpretation of these records requires an accurate depth-age relationship. Here, we present the SPICEcore (SP19) timescale for the age of the ice of SPICEcore. SP19 is synchronized to the WD2014 chronology from the West Antarctic Ice Sheet Divide (WAIS Divide) ice core using stratigraphic matching of 251 volcanic events. These events indicate an age of 54 302±519 BP (years before 1950) at the bottom of SPICEcore. Annual layers identified in sodium and magnesium ions to 11 341 BP were used to interpolate between stratigraphic volcanic tie points, yielding an annually resolved chronology through the Holocene. Estimated timescale uncertainty during the Holocene is less than 18 years relative to WD2014, with the exception of the interval between 1800 to 3100 BP when uncertainty estimates reach ±25 years due to widely spaced volcanic tie points. Prior to the Holocene, uncertainties remain within 124 years relative to WD2014. Results show an average Holocene accumulation rate of 7.4 cm yr-1 (water equivalent). The time variability of accumulation rate is consistent with expectations for steady-state ice flow through the modern spatial pattern of accumulation rate. Time variations in nitrate concentration, nitrate seasonal amplitude and δ15N of N2 in turn are as expected for the accumulation rate variations. The highly variable yet well-constrained Holocene accumulation history at the site can help improve scientific understanding of deposition-sensitive climate proxies such as δ15N of N2 and photolyzed chemical compounds.

Published
2019

3. Aromatic acids in a Eurasian Arctic ice core: A 2600-year proxy record of biomass burning

Author

Grieman, MM, Aydin, M, Fritzsche, D, McConnell, JR, Opel, T, Sigl, M, and Saltzman, ES

Subjects
Physical Geography and Environmental Geoscience, Paleontology
Abstract

Wildfires and their emissions have significant impacts on ecosystems, climate, atmospheric chemistry, and carbon cycling. Well-dated proxy records are needed to study the long-term climatic controls on biomass burning and the associated climate feedbacks. There is a particular lack of information about long-term biomass burning variations in Siberia, the largest forested area in the Northern Hemisphere. In this study we report analyses of aromatic acids (vanillic and para-hydroxybenzoic acids) over the past 2600 years in the Eurasian Arctic Akademii Nauk ice core. These compounds are aerosol-borne, semi-volatile organic compounds derived from lignin combustion. The analyses were made using ion chromatography with electrospray mass spectrometric detection. The levels of these aromatic acids ranged from below the detection limit (0.01 to 0.05 ppb; 1 ppb = 1000 ng L-1) to about 1 ppb, with roughly 30% of the samples above the detection limit. In the preindustrial late Holocene, highly elevated aromatic acid levels are observed during three distinct periods (650-300 BCE, 340-660 CE, and 1460-1660 CE). The timing of the two most recent periods coincides with the episodic pulsing of ice-rafted debris in the North Atlantic known as Bond events and a weakened Asian monsoon, suggesting a link between fires and large-scale climate variability on millennial timescales. Aromatic acid levels also are elevated during the onset of the industrial period from 1780 to 1860 CE, but with a different ratio of vanillic and para-hydroxybenzoic acid than is observed during the preindustrial period. This study provides the first millennial-scale record of aromatic acids. This study clearly demonstrates that coherent aromatic acid signals are recorded in polar ice cores that can be used as proxies for past trends in biomass burning.

Published
2017

5. Observing and modeling the influence of layering on bubble trapping in polar firn

Author

Mitchell, LE, Buizert, C, Brook, EJ, Breton, DJ, Fegyveresi, J, Baggenstos, D, Orsi, A, Severinghaus, J, Alley, RB, Albert, M, Rhodes, RH, McConnell, JR, Sigl, M, Maselli, O, Gregory, S, and Ahn, J

Subjects
firn, layering, ice core, methane, firn density, total air content, Meteorology & Atmospheric Sciences
Abstract

Interpretation of ice core trace gas records depends on an accurate understanding of the processes that smooth the atmospheric signal in the firn. Much work has been done to understand the processes affecting air transport in the open pores of the firn, but a paucity of data from air trapped in bubbles in the firn-ice transition region has limited the ability to constrain the effect of bubble closure processes. Here we present high-resolution measurements of firn density, methane concentrations, nitrogen isotopes, and total air content that show layering in the firn-ice transition region at the West Antarctic Ice Sheet (WAIS) Divide ice core site. Using the notion that bubble trapping is a stochastic process, we derive a new parameterization for closed porosity that incorporates the effects of layering in a steady state firn modeling approach. We include the process of bubble trapping into an open-porosity firn air transport model and obtain a good fit to the firn core data. We find that layering broadens the depth range over which bubbles are trapped, widens the modeled gas age distribution of air in closed bubbles, reduces the mean gas age of air in closed bubbles, and introduces stratigraphic irregularities in the gas age scale that have a peak-to-peak variability of ~10 years at WAIS Divide. For a more complete understanding of gas occlusion and its impact on ice core records, we suggest that this experiment be repeated at sites climatically different from WAIS Divide, for example, on the East Antarctic plateau.

Published
2015

6. The WAIS Divide deep ice core WD2014 chronology – Part 1: Methane synchronization (68–31 ka BP) and the gas age–ice age difference

Author

Buizert, C, Cuffey, KM, Severinghaus, JP, Baggenstos, D, Fudge, TJ, Steig, EJ, Markle, BR, Winstrup, M, Rhodes, RH, Brook, EJ, Sowers, TA, Clow, GD, Cheng, H, Edwards, RL, Sigl, M, McConnell, JR, and Taylor, KC

Subjects
Earth Sciences, Physical Geography and Environmental Geoscience, Geology, Climate Action, Paleontology, Climate change science
Abstract

The West Antarctic Ice Sheet Divide (WAIS Divide, WD) ice core is a newly drilled, high-accumulation deep ice core that provides Antarctic climate records of the past ~68 ka at unprecedented temporal resolution. The upper 2850 m (back to 31.2 ka BP) have been dated using annual-layer counting. Here we present a chronology for the deep part of the core (67.8-31.2 ka BP), which is based on stratigraphic matching to annual-layer-counted Greenland ice cores using globally well-mixed atmospheric methane. We calculate the WD gas age-ice age difference (Δage) using a combination of firn densification modeling, ice-flow modeling, and a data set of δ15N-N2, a proxy for past firn column thickness. The largest Δage at WD occurs during the Last Glacial Maximum, and is 525 ± 120 years. Internally consistent solutions can be found only when assuming little to no influence of impurity content on densification rates, contrary to a recently proposed hypothesis. We synchronize the WD chronology to a linearly scaled version of the layer-counted Greenland Ice Core Chronology (GICC05), which brings the age of Dansgaard-Oeschger (DO) events into agreement with the U/Th absolutely dated Hulu Cave speleothem record. The small Δage at WD provides valuable opportunities to investigate the timing of atmospheric greenhouse gas variations relative to Antarctic climate, as well as the interhemispheric phasing of the "bipolar seesaw".

Published
2015

7. The WAIS-Divide deep ice core WD2014 chronology – Part 2: Methane synchronization (68–31 ka BP) and the gas age-ice age difference

Author

Buizert, C, Cuffey, KM, Severinghaus, JP, Baggenstos, D, Fudge, TJ, Steig, EJ, Markle, BR, Winstrup, M, Rhodes, RH, Brook, EJ, Sowers, TA, Clow, GD, Cheng, H, Edwards, RL, Sigl, M, McConnell, JR, and Taylor, KC

Subjects
Climate Action
Abstract

Abstract. The West Antarctic Ice Sheet (WAIS)-Divide ice core (WAIS-D) is a newly drilled, high-accumulation deep ice core that provides Antarctic climate records of the past ∼68 ka at unprecedented temporal resolution. The upper 2850 m (back to 31.2 ka BP) have been dated using annual-layer counting. Here we present a chronology for the deep part of the core (67.8–31.2 ka BP), which is based on stratigraphic matching to annual-layer-counted Greenland ice cores using globally well-mixed atmospheric methane. We calculate the WAIS-D gas age-ice age difference (Δage) using a combination of firn densification modeling, ice flow modeling, and a dataset of δ15N-N2, a proxy for past firn column thickness. The largest Δage at WAIS-D occurs during the last glacial maximum, and is 525 ± 100 years. Internally consistent solutions can only be found when assuming little-to-no influence of impurity content on densification rates, contrary to a recently proposed hypothesis. We synchronize the WAIS-D chronology to a linearly scaled version of the layer-counted Greenland Ice Core Chronology (GICC05), which brings the age of Dansgaard-Oeschger (DO) events into agreement with the U/Th absolutely dated Hulu speleothem record. The small Δage at WAIS-D provides valuable opportunities to investigate the timing of atmospheric greenhouse gas variations relative to Antarctic climate, as well as the interhemispheric phasing of the bipolar "seesaw".

Published
2014

8. Antarctic-wide array of high-resolution ice core records reveals pervasive lead pollution began in 1889 and persists today.

Author

McConnell, J, Maselli, O, Sigl, M, Vallelonga, P, Neumann, T, Anschütz, H, Curran, M, Das, S, Edwards, R, Kipfstuhl, S, Layman, L, Thomas, E, and Bales, Roger

Subjects
Antarctic Regions, Ecosystem, Environmental Pollution, History, 19th Century, History, 20th Century, History, 21st Century, Humans, Ice, Lead, Water Pollutants, Chemical
Abstract

Interior Antarctica is among the most remote places on Earth and was thought to be beyond the reach of human impacts when Amundsen and Scott raced to the South Pole in 1911. Here we show detailed measurements from an extensive array of 16 ice cores quantifying substantial toxic heavy metal lead pollution at South Pole and throughout Antarctica by 1889 - beating polar explorers by more than 22 years. Unlike the Arctic where lead pollution peaked in the 1970s, lead pollution in Antarctica was as high in the early 20(th) century as at any time since industrialization. The similar timing and magnitude of changes in lead deposition across Antarctica, as well as the characteristic isotopic signature of Broken Hill lead found throughout the continent, suggest that this single emission source in southern Australia was responsible for the introduction of lead pollution into Antarctica at the end of the 19(th) century and remains a significant source today. An estimated 660 t of industrial lead have been deposited over Antarctica during the past 130 years as a result of mid-latitude industrial emissions, with regional-to-global scale circulation likely modulating aerosol concentrations. Despite abatement efforts, significant lead pollution in Antarctica persists into the 21(st) century.

Published
2014

9. Antarctic-wide array of high-resolution ice core records reveals pervasive lead pollution began in 1889 and persists today.

Author

McConnell, JR, Maselli, OJ, Sigl, M, Vallelonga, P, Neumann, T, Anschütz, H, Bales, RC, Curran, MAJ, Das, SB, Edwards, R, Kipfstuhl, S, Layman, L, and Thomas, ER

Subjects
Humans, Lead, Water Pollutants, Chemical, Ecosystem, Ice, Environmental Pollution, History, 19th Century, History, 20th Century, History, 21st Century, Antarctic Regions, Water Pollutants, Chemical, History, 19th Century, 20th Century, 21st Century, Biochemistry and Cell Biology, Other Physical Sciences
Abstract

Interior Antarctica is among the most remote places on Earth and was thought to be beyond the reach of human impacts when Amundsen and Scott raced to the South Pole in 1911. Here we show detailed measurements from an extensive array of 16 ice cores quantifying substantial toxic heavy metal lead pollution at South Pole and throughout Antarctica by 1889 - beating polar explorers by more than 22 years. Unlike the Arctic where lead pollution peaked in the 1970s, lead pollution in Antarctica was as high in the early 20(th) century as at any time since industrialization. The similar timing and magnitude of changes in lead deposition across Antarctica, as well as the characteristic isotopic signature of Broken Hill lead found throughout the continent, suggest that this single emission source in southern Australia was responsible for the introduction of lead pollution into Antarctica at the end of the 19(th) century and remains a significant source today. An estimated 660 t of industrial lead have been deposited over Antarctica during the past 130 years as a result of mid-latitude industrial emissions, with regional-to-global scale circulation likely modulating aerosol concentrations. Despite abatement efforts, significant lead pollution in Antarctica persists into the 21(st) century.

Published
2014

12. Long-lasting cold periods in the mid to late-Holocene

Author

Van Dijk, E., Jungclaus, J., Sigl, M., Timmreck, C., and Krüger, K.

Abstract

From paleoproxy reconstructions and climate model simulations of the Northern Hemisphere (NH) climate during the Common Era (CE), we know that strong volcanic eruptions have induced cold periods like the Little Ice Age (LIA) and the mid-6th century cooling. However, less is known about such cold periods during the Holocene. Here, we study the Max Planck Institute Earth System Model Holocene simulations (6000 BCE to 1850 CE). One of the runs is forced with orbital forcing, land cover, greenhouse gas concentrations, solar forcing, stratospheric ozone, and volcanic forcing. The other run includes only orbital forcing and greenhouse gas concentrations. We simulate a large number of extremely cold years in the all-forcing run, which is primarily explained by volcanic eruptions. Applying a 200-year filter reveals 11 long-lasting cold periods similar to the LIA during the mid to late-Holocene, occurring every once or twice per millennium. These long-lasting cold periods correspond to increased volcanic activity, where the clustering of volcanic eruptions leads to an integrated cooling effect through the slow ocean-sea ice response. Eight of the eleven multi-centennial cold periods in our simulation correspond to previously identified phases of glacier advances throughout the NH, as well as reduced ring widths in tree ring records from Northern Finland. Whereas previous studies used mostly local proxy reconstructions, we identify NH annual mean multi-centennial cold periods. Finding several more such cold periods highlights the importance of understanding volcanic-induced long-lasting cold periods and the impact they could have had on society in the past., The 28th IUGG General Assembly (IUGG2023) (Berlin 2023)

Published
2023
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13. Temperature and Snowfall in Western Queen Maud Land Increasing Faster than Climate Model Projections

Author

Medley, B, McConnell, J. R, Neumann, T. A, Reijmer, C. H, Chellman, N, Sigl, M, and Kipfstuhl, S

Subjects
Meteorology And Climatology
Abstract

East Antarctic Ice Sheet (EAIS) mass balance is largely driven by snowfall. Recently, increased snowfall in Queen Maud Land led to years of EAIS mass gain. It is difficult to determine whether these years of enhanced snowfall are anomalous or part of a longer-term trend, reducing our ability to assess the mitigating impact of snowfall on sea level rise. We determine that the recent snowfall increases in western Queen Maud Land (QML) are part of a long-term trend (+5.2 +/- 3.7% decade(exp -1)) and are unprecedented over the past two millennia. Warming between 1998 and 2016 is significant and rapid (+1.1 +/- 0.7 C decade(exp -1)). Using these observations, we determine that the current accumulation and temperature increases in QML from an ensemble of global climate simulations are too low, which suggests that projections of the QML contribution to sea level rise are potentially overestimated with a reduced mitigating impact of enhanced snowfall in a warming world.

Published
2017
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14. Timing and climate forcing of volcanic eruptions for the past 2,500 years

Author

Sigl, M., Winstrup, M., McConnell, J.R., Welten, K.C., Plunkett, G., Ludlow, F., Buntgen, U., Caffee, M., Chellman, N., Dahl-Jensen, D., Fischer, H., Kipfstuhl, S., Kostick, C., Maselli, O.J., Mekhaldi, F., Mulvaney, R., Muscheler, R., Pasteris, D.R., Pilcher, J.R., Salzer, M., Schupbach, S., Steffensen, J.P., Vinther, B.M., and Woodruff, T.E.

Subjects
Volcanoes, Aerosols, Environmental issues, Science and technology, Zoology and wildlife conservation
Abstract

Volcanic eruptions contribute to climate variability, but quantifying these contributions has been limited by inconsistencies in the timing of atmospheric volcanic aerosol loading determined from ice cores and subsequent cooling from climate proxies such as tree rings. Here we resolve these inconsistencies and show that large eruptions in the tropics and high latitudes were primary drivers of interannual-to-decadal temperature variability in the Northern Hemisphere during the past 2,500 years. Our results are based on new records of atmospheric aerosol loading developed from high-resolution, multi-parameter measurements from an array of Greenland and Antarctic ice cores as well as distinctive age markers to constrain chronologies. Overall, cooling was proportional to the magnitude of volcanic forcing and persisted for up to ten years after some of the largest eruptive episodes. Our revised timescale more firmly implicates volcanic eruptions as catalysts in the major sixth-century pandemics, famines, and socioeconomic disruptions in Eurasia and Mesoamerica while allowing multi-millennium quantification of climate response to volcanic forcing., Volcanic eruptions are primary drivers of natural climate variability--their sulfate aerosol injections into the stratosphere shield the Earth's surface from incoming solar radiation, leading to short-term cooling at regional-to-global scales [...]

Published
2015
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15. Diabetisches Fußsyndrom – Teil 1

Author

Rümenapf, G., Morbach, S., Rother, U., Uhl, C., Görtz, H., Böckler, D., Behrendt, C.‑A., Hochlenert, D., Engels, G., and Sigl, M.

Subjects
Diabetisches Fußsyndrom, Diabetic polyneuropathy, Foot, Diabetic foot syndrome, Amputation, Surgical, Diabetic Foot, Diabetische Polyneuropathie, Periphere arterielle Verschlusskrankheit, Peripheral arterial occlusive disease, Diabetes mellitus, Germany, CME, Humans, Amputation, Vascular Surgical Procedures
Abstract

There are ca. 8 million persons with diabetes mellitus living in Germany. A late sequelae of diabetes is the diabetic foot syndrome (DFS), the prevalence of which is greatly increasing. It comprises all alterations of the foot as a result of diabetic polyneuropathy as well as microvascular and macrovascular (peripheral arterial occlusive disease, PAOD) alterations. Many of the ca. 250,000 newly diagnosed diabetic foot ulcers per year become chronic wounds. Despite intensive efforts for prevention, early diagnosis and adequate wound care, ca. 13,000 persons with diabetes undergo major limb amputation in Germany every year. With consistent treatment in interdisciplinary centers and by exhausting all possible methods of wound treatment, pressure relief as well as arterial revascularization, the major amputation rate in patients with diabetic foot problems can be reduced by 80%. With a suitable strategy of prevention, the recurrence rate of foot ulcers would be reduced.In Deutschland leben ca. 8 Mio. Menschen mit Diabetes mellitus. Eine Spätfolge dieser Erkrankung ist das diabetische Fußsyndrom (DFS), dessen Prävalenz stark ansteigt. Es umfasst alle Veränderungen am Fuß als Folge der diabetischen Polyneuropathie sowie mikro- und makroangiopathischer (periphere arterielle Verschlusskrankheit, PAVK) Veränderungen. Jährlich entstehen ca. 250.000 neue diabetische Fußulzera. Diese werden oft zu chronischen Wunden. Trotz intensiver Bemühungen um Prävention, frühzeitige Diagnostik und stadiengerechte Wundbehandlung werden in Deutschland jährlich ca. 13.000 Majoramputationen bei Diabetikern durchgeführt. Bei konsequenter Therapie des DFS in interdisziplinären Zentren mit Ausschöpfung aller Möglichkeiten der Wundbehandlung, der Druckentlastung sowie einer arteriellen Revaskularisation kann die Majoramputationsrate um bis zu 80 % gesenkt werden. Durch eine geeignete Präventionsstrategie wäre die große Gefahr der Rezidivulzera geringer.

Published
2020

20. Improved estimates of preindustrial biomass burning reduce the magnitude of aerosol climate forcing in the Southern Hemisphere.

Author

Liu, P., Kaplan, J.O., Mickley, L.J., Li, Y., Chellman, N.J., Arienzo, M.M., Kodros, J.K., Pierce, J.R., Sigl, M., Frietag, J., Mulvaney, R., Curran, M.A.J., McConnell, J.R., Liu, P., Kaplan, J.O., Mickley, L.J., Li, Y., Chellman, N.J., Arienzo, M.M., Kodros, J.K., Pierce, J.R., Sigl, M., Frietag, J., Mulvaney, R., Curran, M.A.J., and McConnell, J.R.

Abstract

Fire plays a pivotal role in shaping terrestrial ecosystems and the chemical composition of the atmosphere and thus influences Earth’s climate. The trend and magnitude of fire activity over the past few centuries are controversial, which hinders understanding of preindustrial to present-day aerosol radiative forcing. Here, we present evidence from records of 14 Antarctic ice cores and 1 central Andean ice core, suggesting that historical fire activity in the Southern Hemisphere (SH) exceeded present-day levels. To understand this observation, we use a global fire model to show that overall SH fire emissions could have declined by 30% over the 20th century, possibly because of the rapid expansion of land use for agriculture and animal production in middle to high latitudes. Radiative forcing calculations suggest that the decreasing trend in SH fire emissions over the past century largely compensates for the cooling effect of increasing aerosols from fossil fuel and biofuel sources.

Published
2021

21. Volcanic climate forcing preceding the inception of the Younger Dryas:Implications for tracing the Laacher See eruption

Author

Abbott, P. M., Niemeier, U., Timmreck, C., Riede, F., McConnell, J. R., Severi, M., Fischer, H., Svensson, A., Toohey, M., Reinig, F., Sigl, M., Abbott, P. M., Niemeier, U., Timmreck, C., Riede, F., McConnell, J. R., Severi, M., Fischer, H., Svensson, A., Toohey, M., Reinig, F., and Sigl, M.

Abstract

Climatic warming from the last glacial maximum to the current interglacial period was punctuated by a similar to 1300 years long cold period, commonly referred to as the Younger Dryas (YD). Several hypotheses have been proposed for the mechanism triggering the abrupt inception of the YD, including freshwater forcing, an extra-terrestrial impact, and aerosols from volcanic eruptions. Here, we use synchronised sulphate and sulphur records from both Greenland and Antarctic ice cores to reconstruct volcanic forcing between 13,200-12,800 a BPGICC05 (years before 1950 CE on the Greenland Ice Core Chronology 2005; GICC05). This continuous reconstruction of stratospheric sulphur injections highlights a -110-year cluster of four major bipolar volcanic signals alongside several smaller events just prior to the YD inception. The cumulative Northern Hemisphere aerosol burden and radiative forcing from this cluster exceeds the most volcanically active periods during the Common Era, which experienced notable multidecadal scale cooling commonly attributed to volcanic effects. The Laacher See eruption (LSE), recently redated to 13,006 +/- 9 cal a BP, falls within our time window of study and has been proposed as a trigger for the YD but a direct volcanic imprint for the LSE in the Greenland ice cores has thus far proved elusive. Comparison of simulated sulphate deposition for mid- and high-sulphur LSE-type emission scenarios to the ice-core estimated sulphate deposition and interhemispheric asymmetry ratios allows several signals between 13,025 and 12,975 a BPGICC05 to be proposed as plausible candidates for the LSE. The magnitude and persistence of volcanic forcing directly preceding the YD inception highlights the need to consider stratospheric sulphur injections and their radiative forcing in future analyses and climate model experiments used to explore the mechanisms that triggered this or similar abrupt cooling events. (C) 2021 The Authors. Published by Elsevier Ltd.

Published
2021

23. The magnitude and impact of the 431 CE Tierra Blanca Joven eruption of Ilopango, El Salvador

Author

Secretaría de Medio Ambiente y Recursos Naturales (México), European Research Council, Natural Environment Research Council (UK), Pedrazzi, Dario [0000-0002-6869-1325], Smith, V. C., Costa, A., Aguirre-Díaz, Gerardo, Pedrazzi, Dario, Scifo, A., Plunkett, G., Poret, M., Tournigand, P. Y., Miles, D., Dee, M. W., McConnell, J. R., Sunyé-Puchol, I., Harris, Pablo Davila, Sigl, M., Pilcher, J. R., Chellman, N., Gutierrez, E., Secretaría de Medio Ambiente y Recursos Naturales (México), European Research Council, Natural Environment Research Council (UK), Pedrazzi, Dario [0000-0002-6869-1325], Smith, V. C., Costa, A., Aguirre-Díaz, Gerardo, Pedrazzi, Dario, Scifo, A., Plunkett, G., Poret, M., Tournigand, P. Y., Miles, D., Dee, M. W., McConnell, J. R., Sunyé-Puchol, I., Harris, Pablo Davila, Sigl, M., Pilcher, J. R., Chellman, N., and Gutierrez, E.

Abstract

The Tierra Blanca Joven (TBJ) eruption from Ilopango volcano deposited thick ash over much of El Salvador when it was inhabited by the Maya, and rendered all areas within at least 80 km of the volcano uninhabitable for years to decades after the eruption. Nonetheless, the more widespread environmental and climatic impacts of this large eruption are not well known because the eruption magnitude and date are not well constrained. In this multifaceted study we have resolved the date of the eruption to 431 ± 2 CE by identifying the ash layer in a well-dated, high-resolution Greenland ice-core record that is >7,000 km from Ilopango; and calculated that between 37 and 82 km3 of magma was dispersed from an eruption coignimbrite column that rose to ∼45 km by modeling the deposit thickness using state-of-the-art tephra dispersal methods. Sulfate records from an array of ice cores suggest stratospheric injection of 14 ± 2 Tg S associated with the TBJ eruption, exceeding those of the historic eruption of Pinatubo in 1991. Based on these estimates it is likely that the TBJ eruption produced a cooling of around 0.5 °C for a few years after the eruption. The modeled dispersal and higher sulfate concentrations recorded in Antarctic ice cores imply that the cooling would have been more pronounced in the Southern Hemisphere. The new date confirms the eruption occurred within the Early Classic phase when Maya expanded across Central America.

Published
2020

28. Multi-model comparison of the volcanic sulfate deposition from the 1815 eruption of Mt. Tambora

Author

Marshall, L., Schmidt, A., Toohey, M., Carslaw, K. S., Mann, G. W., Sigl, M., Khodri, Myriam, Timmreck, C., Zanchettin, D., Ball, W. T., Bekki, S., Brooke, J. S. A., Dhomse, S., Johnson, C., Lamarque, J. F., LeGrande, A. N., Mills, M. J., Niemeier, U., Pope, J. O., Poulain, V., Robock, A., Rozanov, E., Stenke, A., Sukhodolov, T., Tilmes, S., Tsigaridis, K., Tummon, F., Institute for Climate and Atmospheric Science [Leeds] (ICAS), School of Earth and Environment [Leeds] (SEE), University of Leeds-University of Leeds, Leibniz-Institut für Meereswissenschaften (IFM-GEOMAR), Max-Planck-Institut für Meteorologie (MPI-M), Max-Planck-Gesellschaft, National Centre for Atmospheric Science [Leeds] (NCAS), Natural Environment Research Council (NERC), Laboratory of Environmental Chemistry [Villigen] (LUC), Paul Scherrer Institute (PSI), Océan et variabilité du climat (VARCLIM), Laboratoire d'Océanographie et du Climat : Expérimentations et Approches Numériques (LOCEAN), Muséum national d'Histoire naturelle (MNHN)-Institut de Recherche pour le Développement (IRD)-Institut national des sciences de l'Univers (INSU - CNRS)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), École normale supérieure - Paris (ENS-PSL), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Université Paris Cité (UPCité)-École normale supérieure - Paris (ENS-PSL), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Université Paris Cité (UPCité)-Muséum national d'Histoire naturelle (MNHN)-Institut de Recherche pour le Développement (IRD)-Institut national des sciences de l'Univers (INSU - CNRS)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Université Paris Cité (UPCité), Max Planck Institute for Meteorology (MPI-M), Department of Environmental Sciences, Informatics and Statistics [Venezia], University of Ca’ Foscari [Venice, Italy], Institute for Atmospheric and Climate Science [Zürich] (IAC), Eidgenössische Technische Hochschule - Swiss Federal Institute of Technology [Zürich] (ETH Zürich), Physikalisch-Meteorologisches Observatorium Davos/World Radiation Center (PMOD/WRC), STRATO - LATMOS, Laboratoire Atmosphères, Milieux, Observations Spatiales (LATMOS), Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Institut national des sciences de l'Univers (INSU - CNRS)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Institut national des sciences de l'Univers (INSU - CNRS)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS), School of Chemistry [Leeds], University of Leeds, Met Office Hadley Centre for Climate Change (MOHC), United Kingdom Met Office [Exeter], Atmospheric Chemistry Observations and Modeling Laboratory (ACOML), National Center for Atmospheric Research [Boulder] (NCAR), NASA Goddard Space Flight Center (GSFC), British Antarctic Survey (BAS), Processus de la variabilité climatique tropicale et impacts (PARVATI), Muséum national d'Histoire naturelle (MNHN)-Institut de Recherche pour le Développement (IRD)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-École normale supérieure - Paris (ENS-PSL), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Muséum national d'Histoire naturelle (MNHN)-Institut de Recherche pour le Développement (IRD)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS), Department of Environmental Sciences [New Brunswick], School of Environmental and Biological Sciences [New Brunswick], Rutgers, The State University of New Jersey [New Brunswick] (RU), Rutgers University System (Rutgers)-Rutgers University System (Rutgers)-Rutgers, The State University of New Jersey [New Brunswick] (RU), Rutgers University System (Rutgers)-Rutgers University System (Rutgers), NASA Goddard Institute for Space Studies (GISS), Center for Climate Systems Research [New York] (CCSR), Columbia University [New York], The Arctic University of Norway [Tromsø, Norway] (UiT), US National Science Foundation grant AGS-1430051, German Federal Ministry of Education and Research (BMBF), research program 'MiKliP' (FKZ: 01LP1517B, Swiss National Science Foundation grant 20F121_138017, NERC grant NEK/K012150/1, ANR-10-LABX-0018,L-IPSL,LabEx Institut Pierre Simon Laplace (IPSL): Understand climate and anticipate future changes(2010), European Project: 603557,EC:FP7:ENV,FP7-ENV-2013-two-stage,STRATOCLIM(2013), Institut de Recherche pour le Développement (IRD)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Muséum national d'Histoire naturelle (MNHN)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), École normale supérieure - Paris (ENS Paris), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-École normale supérieure - Paris (ENS Paris), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Institut de Recherche pour le Développement (IRD)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Muséum national d'Histoire naturelle (MNHN)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), Sorbonne Université (SU)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Sorbonne Université (SU)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS), and The Arctic University of Norway (UiT)

Subjects
[SDU.STU.VO]Sciences of the Universe [physics]/Earth Sciences/Volcanology, Settore GEO/12 - Oceanografia e Fisica dell'Atmosfera
Abstract

Source at https://doi.org/10.5194/acp-18-2307-2018. The eruption of Mt. Tambora in 1815 was the largest volcanic eruption of the past 500 years. The eruption had significant climatic impacts, leading to the 1816 "year without a summer", and remains a valuable event from which to understand the climatic effects of large stratospheric volcanic sulfur dioxide injections. The eruption also resulted in one of the strongest and most easily identifiable volcanic sulfate signals in polar ice cores, which are widely used to reconstruct the timing and atmospheric sulfate loading of past eruptions. As part of the Model Intercomparison Project on the climatic response to Volcanic forcing (VolMIP), five state-of-the-art global aerosol models simulated this eruption. We analyse both simulated background (no Tambora) and volcanic (with Tambora) sulfate deposition to polar regions and compare to ice core records. The models simulate overall similar patterns of background sulfate deposition, although there are differences in regional details and magnitude. However, the volcanic sulfate deposition varies considerably between the models with differences in timing, spatial pattern and magnitude. Mean simulated deposited sulfate on Antarctica ranges from 19 to 264 kg km−2 and on Greenland from 31 to 194 kg km−2, as compared to the mean ice-core-derived estimates of roughly 50 kg km−2 for both Greenland and Antarctica. The ratio of the hemispheric atmospheric sulfate aerosol burden after the eruption to the average ice sheet deposited sulfate varies between models by up to a factor of 15. Sources of this inter-model variability include differences in both the formation and the transport of sulfate aerosol. Our results suggest that deriving relationships between sulfate deposited on ice sheets and atmospheric sulfate burdens from model simulations may be associated with greater uncertainties than previously thought.

Published
2018

29. Erratum to: Tree rings reveal globally coherent signature of cosmogenic radiocarbon events in 774 and 993 CE (Nature Communications, (2018), 9, 1, (3605), 10.1038/s41467-018-06036-0)

Author

Büntgen, U, Wacker, L, Galván, JD, Arnold, S, Arseneault, D, Baillie, M, Beer, J, Bernabei, M, Bleicher, N, Boswijk, G, Bräuning, A, Carrer, M, Ljungqvist, FC, Cherubini, P, Christl, M, Christie, DA, Clark, PW, Cook, ER, D’Arrigo, R, Davi, N, Eggertsson, Ó, Esper, J, Fowler, AM, Gedalof, Z, Gennaretti, F, Grießinger, J, Grissino-Mayer, H, Grudd, H, Gunnarson, BE, Hantemirov, R, Herzig, F, Hessl, A, Heussner, KU, Jull, AJT, Kukarskih, V, Kirdyanov, A, Kolář, T, Krusic, PJ, Kyncl, T, Lara, A, LeQuesne, C, Linderholm, HW, Loader, NJ, Luckman, B, Miyake, F, Myglan, VS, Nicolussi, K, Oppenheimer, C, Palmer, J, Panyushkina, I, Pederson, N, Rybníček, M, Schweingruber, FH, Seim, A, Sigl, M, Churakova (Sidorova), O, Speer, JH, Synal, HA, Tegel, W, Treydte, K, Villalba, R, Wiles, G, Wilson, R, Winship, LJ, Wunder, J, Yang, B, Young, GHF, Büntgen, U, Wacker, L, Galván, JD, Arnold, S, Arseneault, D, Baillie, M, Beer, J, Bernabei, M, Bleicher, N, Boswijk, G, Bräuning, A, Carrer, M, Ljungqvist, FC, Cherubini, P, Christl, M, Christie, DA, Clark, PW, Cook, ER, D’Arrigo, R, Davi, N, Eggertsson, Ó, Esper, J, Fowler, AM, Gedalof, Z, Gennaretti, F, Grießinger, J, Grissino-Mayer, H, Grudd, H, Gunnarson, BE, Hantemirov, R, Herzig, F, Hessl, A, Heussner, KU, Jull, AJT, Kukarskih, V, Kirdyanov, A, Kolář, T, Krusic, PJ, Kyncl, T, Lara, A, LeQuesne, C, Linderholm, HW, Loader, NJ, Luckman, B, Miyake, F, Myglan, VS, Nicolussi, K, Oppenheimer, C, Palmer, J, Panyushkina, I, Pederson, N, Rybníček, M, Schweingruber, FH, Seim, A, Sigl, M, Churakova (Sidorova), O, Speer, JH, Synal, HA, Tegel, W, Treydte, K, Villalba, R, Wiles, G, Wilson, R, Winship, LJ, Wunder, J, Yang, B, and Young, GHF

Abstract

The original version of this Article contained an error in the Data Availability section, which incorrectly read ‘All data will be freely available via https://www.ams.ethz.ch/research.html.’ The correct version states ‘http://www.ams.ethz.ch/research/published-data.html’ in place of ‘https://www.ams.ethz.ch/research.html’. This has been corrected in both the PDF and HTML versions of the Article.

Published
2018

30. Tree rings reveal globally coherent signature of cosmogenic radiocarbon events in 774 and 993 CE

Author

Büntgen, U, Wacker, L, Galván, JD, Arnold, S, Arseneault, D, Baillie, M, Beer, J, Bernabei, M, Bleicher, N, Boswijk, G, Bräuning, A, Carrer, M, Ljungqvist, FC, Cherubini, P, Christl, M, Christie, DA, Clark, PW, Cook, ER, D’arrigo, R, Davi, N, Eggertsson, Ó, Esper, J, Fowler, AM, Gedalof, Z, Gennaretti, F, Grießinger, J, Grissino-Mayer, H, Grudd, H, Gunnarson, BE, Hantemirov, R, Herzig, F, Hessl, A, Heussner, K-U, Jull, AJT, Kukarskih, V, Kirdyanov, A, KoláŖ, TVS, Krusic, PJ, Kyncl, TVS, Lara, A, LeQuesne, C, Linderholm, HW, Loader, NJ, Luckman, B, Miyake, F, Myglan, VS, Nicolussi, K, Oppenheimer, C, Palmer, J, Panyushkina, I, PEDERSON, N, Rybníček, M, Schweingruber, FH, Seim, A, Sigl, M, Sidorova, OC, Speer, JH, Synal, H-A, Tegel, W, Treydte, K, Villalba, R, Wiles, G, Wilson, R, Winship, LJ, Wunder, J, Yang, B, Young, GHF, Büntgen, U, Wacker, L, Galván, JD, Arnold, S, Arseneault, D, Baillie, M, Beer, J, Bernabei, M, Bleicher, N, Boswijk, G, Bräuning, A, Carrer, M, Ljungqvist, FC, Cherubini, P, Christl, M, Christie, DA, Clark, PW, Cook, ER, D’arrigo, R, Davi, N, Eggertsson, Ó, Esper, J, Fowler, AM, Gedalof, Z, Gennaretti, F, Grießinger, J, Grissino-Mayer, H, Grudd, H, Gunnarson, BE, Hantemirov, R, Herzig, F, Hessl, A, Heussner, K-U, Jull, AJT, Kukarskih, V, Kirdyanov, A, KoláŖ, TVS, Krusic, PJ, Kyncl, TVS, Lara, A, LeQuesne, C, Linderholm, HW, Loader, NJ, Luckman, B, Miyake, F, Myglan, VS, Nicolussi, K, Oppenheimer, C, Palmer, J, Panyushkina, I, PEDERSON, N, Rybníček, M, Schweingruber, FH, Seim, A, Sigl, M, Sidorova, OC, Speer, JH, Synal, H-A, Tegel, W, Treydte, K, Villalba, R, Wiles, G, Wilson, R, Winship, LJ, Wunder, J, Yang, B, and Young, GHF

Abstract

Nature Communications, doi:10.1038/s41467-018-06036-0

Published
2018

32. Diabetisches Fußsyndrom – Teil 2: Revaskularisation, Behandlungsalternativen, Versorgungsstrukturen, Rezidivprophylaxe.

Author

Rümenapf, G., Morbach, S., Rother, U., Uhl, C., Görtz, H., Böckler, D., Behrendt, C. A., Hochlenert, D., Engels, G., Hohneck, A., and Sigl, M.

Abstract

Copyright of Der Chirurg is the property of Springer Nature and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Published
2021
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33. Diabetisches Fußsyndrom – Teil 1: Definition, Pathophysiologie, Diagnostik und Klassifikation.

Author

Rümenapf, G., Morbach, S., Rother, U., Uhl, C., Görtz, H., Böckler, D., Behrendt, C.‑A., Hochlenert, D., Engels, G., and Sigl, M.

Abstract

Copyright of Der Chirurg is the property of Springer Nature and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Published
2021
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34. The PMIP4 contribution to CMIP6 – Part 3: The last millennium, scientific objective, and experimental design for the PMIP4 past1000 simulations

Author

Jungclaus, J. H., Bard, E., Baroni, M., Braconnot, P., Cao, J., Chini, L. P., Egorova, T., Evans, M., González-Rouco, J. F., Goosse, H., Hurtt, G. C., Joos, F., Kaplan, J. O., Khodri, M., Klein Goldewijk, K., Krivova, N., LeGrande, A. N., Lorenz, S. J., Luterbacher, J., Man, W., Maycock, A. C., Meinshausen, M., Moberg, A., Muscheler, R., Nehrbass-Ahles, C., Otto-Bliesner, B. I., Phipps, S. J., Pongratz, J., Rozanov, E., Schmidt, G. A., Schmidt, H., Schmutz, W., Schurer, A., Shapiro, A. I., Sigl, M., Smerdon, J. E., Solanki, S. K., Timmreck, C., Toohey, M., Usoskin, I. G., Wagner, S., Wu, C.-J., Yeo, K. L., Zanchettin, D., Zhang, Q., and Zorita, E.

Subjects
lcsh:Geology, lcsh:QE1-996.5
Abstract

The pre-industrial millennium is among the periods selected by the Paleoclimate Model Intercomparison Project (PMIP) for experiments contributing to the sixth phase of the Coupled Model Intercomparison Project (CMIP6) and the fourth phase of the PMIP (PMIP4). The past1000 transient simulations serve to investigate the response to (mainly) natural forcing under background conditions not too different from today, and to discriminate between forced and internally generated variability on interannual to centennial timescales. This paper describes the motivation and the experimental set-ups for the PMIP4-CMIP6 past1000 simulations, and discusses the forcing agents orbital, solar, volcanic, and land use/land cover changes, and variations in greenhouse gas concentrations. The past1000 simulations covering the pre-industrial millennium from 850 Common Era (CE) to 1849 CE have to be complemented by historical simulations (1850 to 2014 CE) following the CMIP6 protocol. The external forcings for the past1000 experiments have been adapted to provide a seamless transition across these time periods. Protocols for the past1000 simulations have been divided into three tiers. A default forcing data set has been defined for the Tier 1 (the CMIP6 past1000) experiment. However, the PMIP community has maintained the flexibility to conduct coordinated sensitivity experiments to explore uncertainty in forcing reconstructions as well as parameter uncertainty in dedicated Tier 2 simulations. Additional experiments (Tier 3) are defined to foster collaborative model experiments focusing on the early instrumental period and to extend the temporal range and the scope of the simulations. This paper outlines current and future research foci and common analyses for collaborative work between the PMIP and the observational communities (reconstructions, instrumental data).

Published
2017

35. The PMIP4 contribution to CMIP6 – Part 3: the Last Millennium, Scientific Objective and Experimental Design for the PMIP4 past1000 simulations

Author

Jungclaus, J., https://orcid.org/0000-0002-3849-4339, Bard, E., Baroni, M., Braconnot, P., Cao, J., Chini, L., Egorova, T., Evans, M., González-Rouco, J., Goosse, H., Hurtt, G., Joos, F., Kaplan, J., Khodri, M., Klein Goldewijk, K., Krivova, N., LeGrande, A., Lorenz, S., Luterbacher, J., Man, W., Meinshausen, M., Moberg, A., Nehrbass-Ahles, C., Otto-Bliesner, B., Phipps, S., Pongratz, J., https://orcid.org/0000-0003-0372-3960, Rozanov, E., Schmidt, G., Schmidt, H., https://orcid.org/0000-0001-7977-5041, Schmutz, W., Schurer, A., Shapiro, A., Sigl, M., Smerdon, J., Solanki, S., Timmreck, C., Toohey, M., Usoskin, I., Wagner, S., Wu, C., Yeo, K., Zanchettin, D., Zhang, Q., and Zorita, E.

Abstract

The pre-industrial millennium is among the periods selected by the Paleoclimate Model Intercomparison Project (PMIP) for experiments contributing to the sixth phase of the Coupled Model Intercomparison Project (CMIP6) and the fourth phase of the PMIP (PMIP4). The past1000 transient simulations serve to investigate the response to (mainly) natural forcing under background conditions not too different from today, and to discriminate between forced and internally generated variability on interannual to centennial timescales. This paper describes the motivation and the experimental set-ups for the PMIP4-CMIP6 past1000 simulations, and discusses the forcing agents orbital, solar, volcanic, and land use/land cover changes, and variations in greenhouse gas concentrations. The past1000 simulations covering the pre-industrial millennium from 850 Common Era (CE) to 1849 CE have to be complemented by historical simulations (1850 to 2014 CE) following the CMIP6 protocol. The external forcings for the past1000 experiments have been adapted to provide a seamless transition across these time periods. Protocols for the past1000 simulations have been divided into three tiers. A default forcing data set has been defined for the Tier 1 (the CMIP6 past1000) experiment. However, the PMIP community has maintained the flexibility to conduct coordinated sensitivity experiments to explore uncertainty in forcing reconstructions as well as parameter uncertainty in dedicated Tier 2 simulations. Additional experiments (Tier 3) are defined to foster collaborative model experiments focusing on the early instrumental period and to extend the temporal range and the scope of the simulations. This paper outlines current and future research foci and common analyses for collaborative work between the PMIP and the observational communities (reconstructions, instrumental data).

Published
2017

36. Multi-proxy dating of Iceland's major pre-settlement Katla eruption to 822-823 CE

Author

Büntgen, U, Eggertsson, Ó, Wacker, L, Sigl, M, Ljungqvist, FC, di Cosmo, N, Plunkett, G, Krusic, PJ, Newfield, TP, Esper, J, Lane, C, Reinig, F, Oppenheimer, C, Buentgen, Ulf [0000-0002-3821-0818], Krusic, Paul [0000-0001-5358-9697], Lane, Christine [0000-0001-9206-3903], Oppenheimer, Clive [0000-0003-4506-7260], and Apollo - University of Cambridge Repository

Subjects
13 Climate Action, 37 Earth Sciences, 3705 Geology, 3709 Physical Geography and Environmental Geoscience
Abstract

Investigations of the impacts of past volcanic eruptions on climate, environment, and society require accurate chronologies. However, eruptions that are not recorded in historical documents can seldom be dated exactly. Here we use annually resolved radiocarbon ($^{14}$C) measurements to isolate the 775 CE cosmogenic $^{14}$C peak in a subfossil birch tree that was buried by a glacial outburst flood in southern Iceland. We employ this absolute time marker to date a subglacial eruption of Katla volcano at late 822 CE to early 823 CE. We argue for correlation between the 822–823 CE eruption and a conspicuous sulfur anomaly evident in Greenland ice cores, which follows in the wake of an even larger volcanic signal (ca. 818–820 CE) as yet not attributed to a known eruption. An abrupt summer cooling in 824 CE, evident in tree-ring reconstructions for Fennoscandia and the Northern Hemisphere, suggests a climatic response to the Katla eruption. Written historical sources from Europe and China corroborate our proposed tree ring–radiocarbon–ice core linkage but also point to combined effects of eruptions occurring during this period. Our study describes the oldest precisely dated, high-latitude eruption and reveals the impact of an extended phase of volcanic forcing in the early 9$^{th}$ century. It also provides insight into the existence of prehistoric woodland cover and the nature of volcanism several decades before Iceland's permanent settlement began.

Published
2017
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38. The PMIP4 contribution to CMIP6 – Part 3: The last millennium,scientific objective, and experimental design for the PMIP4 past1000 simulations

Author

Jungclaus, J, Bard, E, Baroni, M, Braconnot, P, Cao, J, Chini, LP, Egorova, T, Evans, M, González-Rouco, JF, Goosse, H, Hurtt, GC, Joos, F, Kaplan, JO, Khodri, M, Goldewijk, KK, Krivova, N, LeGrande, AN, Lorenz, SJ, Luterbacher, J, Man, W, Maycock, AC, Meinshausen, M, Moberg, A, Muscheler, R, Nehrbass-Ahles, C, Otto-Bliesner, BI, Phipps, SJ, Pongratz, J, Rozanov, E, Schmidt, GA, Schmidt, H, Schmutz, W, Schurer, A, Shapiro, AI, Sigl, M, Smerdon, JE, Solanki, SK, Timmreck, C, Toohey, M, Usoskin, IG, Wagner, S, Wu, C-J, Yeo, KL, Zanchettin, D, Zhang, Q, Zorita, E, UCL - SST/ELI/ELIC - Earth & Climate, Max-Planck-Institut für Meteorologie (MPI-M), Max-Planck-Gesellschaft, Collège de France - Chaire Evolution du climat et de l'océan, Centre européen de recherche et d'enseignement des géosciences de l'environnement (CEREGE), Institut de Recherche pour le Développement (IRD)-Aix Marseille Université (AMU)-Collège de France (CdF (institution))-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Institut National de Recherche pour l’Agriculture, l’Alimentation et l’Environnement (INRAE)-Institut de Recherche pour le Développement (IRD)-Aix Marseille Université (AMU)-Collège de France (CdF (institution))-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Institut National de Recherche pour l’Agriculture, l’Alimentation et l’Environnement (INRAE), Laboratoire des Sciences du Climat et de l'Environnement [Gif-sur-Yvette] (LSCE), Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris-Saclay-Centre National de la Recherche Scientifique (CNRS), Modelling the Earth Response to Multiple Anthropogenic Interactions and Dynamics (MERMAID), Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris-Saclay-Centre National de la Recherche Scientifique (CNRS)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris-Saclay-Centre National de la Recherche Scientifique (CNRS), Department of Computer Science and Engineering [Shanghai] (CSE), Shanghai Jiao Tong University [Shanghai], Department of Geographical Sciences, University of Maryland [College Park], University of Maryland System-University of Maryland System, Institute for Atmospheric and Climate Science [Zürich] (IAC), Eidgenössische Technische Hochschule - Swiss Federal Institute of Technology [Zürich] (ETH Zürich), University of Maryland System, Instituto de Geociencias [Madrid] (IGEO), Universidad Complutense de Madrid = Complutense University of Madrid [Madrid] (UCM)-Consejo Superior de Investigaciones Científicas [Madrid] (CSIC), Université Catholique de Louvain = Catholic University of Louvain (UCL), Climate and Environmental Physics [Bern] (CEP), Physikalisches Institut [Bern], Universität Bern [Bern] (UNIBE)-Universität Bern [Bern] (UNIBE), Université de Lausanne = University of Lausanne (UNIL), Processus de la variabilité climatique tropicale et impacts (PARVATI), Laboratoire d'Océanographie et du Climat : Expérimentations et Approches Numériques (LOCEAN), Muséum national d'Histoire naturelle (MNHN)-Institut de Recherche pour le Développement (IRD)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), École normale supérieure - Paris (ENS-PSL), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-École normale supérieure - Paris (ENS-PSL), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Muséum national d'Histoire naturelle (MNHN)-Institut de Recherche pour le Développement (IRD)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS), PBL Netherlands Environmental Assessment Agency, Max-Planck-Institut für Sonnensystemforschung = Max Planck Institute for Solar System Research (MPS), NASA Goddard Space Flight Center (GSFC), Department of Geography, Justus-Liebig- University, Justus-Liebig-Universität Gießen = Justus Liebig University (JLU), Laboratory of Numerical Modeling for Atmospheric Sciences and Geophysical Fluid Dynamics (LASG), Institute of Atmospheric Physics [Beijing] (IAP), Chinese Academy of Sciences [Beijing] (CAS)-Chinese Academy of Sciences [Beijing] (CAS), University of Leeds, Potsdam Institute for Climate Impact Research (PIK), Bolin Centre for Climate Research, Stockholm University, Department of Geology [Lund], Lund University [Lund], National Center for Atmospheric Research [Boulder] (NCAR), University of New South Wales [Sydney] (UNSW), Department of Global Ecology [Carnegie] (DGE), Carnegie Institution for Science, NASA Goddard Institute for Space Studies (GISS), Max Planck Institute for Meteorology (MPI-M), Physikalisch-Meteorologisches Observatorium Davos/World Radiation Center (PMOD/WRC), School of Geosciences [Edinburgh], University of Edinburgh, School of Industrial and Systems Engineering [Georgia Tech] (ISyE), Georgia Institute of Technology [Atlanta], Laboratory of Radio- and Environmental Chemistry [Villigen], Paul Scherrer Institute (PSI), Lamont-Doherty Earth Observatory (LDEO), Columbia University [New York], Leibniz-Institut für Meereswissenschaften (IFM-GEOMAR), University of Oulu, Eurecom [Sophia Antipolis], Department of Environmental Sciences, Informatics and Statistics [Venezia], University of Ca’ Foscari [Venice, Italy], Department of Physical Geography [Stockholm], Helmholtz-Zentrum Geesthacht (GKSS), European Project: 603557,EC:FP7:ENV,FP7-ENV-2013-two-stage,STRATOCLIM(2013), Chaire Evolution du climat et de l'océan, Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris-Saclay-Centre National de la Recherche Scientifique (CNRS)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ), Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris-Saclay-Centre National de la Recherche Scientifique (CNRS)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris-Saclay-Centre National de la Recherche Scientifique (CNRS)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ), Universität Bern [Bern]-Universität Bern [Bern], Université de Lausanne (UNIL), Institut de Recherche pour le Développement (IRD)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Muséum national d'Histoire naturelle (MNHN)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), École normale supérieure - Paris (ENS Paris), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-École normale supérieure - Paris (ENS Paris), Université Paris sciences et lettres (PSL)-Université Paris sciences et lettres (PSL)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université Paris Diderot - Paris 7 (UPD7)-École polytechnique (X)-Centre National d'Études Spatiales [Toulouse] (CNES)-Sorbonne Université (SU)-Centre National de la Recherche Scientifique (CNRS)-Institut de Recherche pour le Développement (IRD)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Muséum national d'Histoire naturelle (MNHN)-Institut Pierre-Simon-Laplace (IPSL (FR_636)), Max-Planck-Institut für Sonnensystemforschung (MPS), Justus-Liebig-Universität Gießen (JLU), Carnegie Institution for Science [Washington], Centre National de la Recherche Scientifique (CNRS)-Institut de Recherche pour le Développement (IRD)-Collège de France (CdF)-Institut national des sciences de l'Univers (INSU - CNRS)-Aix Marseille Université (AMU)-Institut National de la Recherche Agronomique (INRA), Université Paris-Saclay-Commissariat à l'énergie atomique et aux énergies alternatives (CEA)-Université de Versailles Saint-Quentin-en-Yvelines (UVSQ)-Centre National de la Recherche Scientifique (CNRS), Eidgenössische Technische Hochschule - Swiss Federal Institute of Technology in Zürich [Zürich] (ETH Zürich), Universidad Complutense de Madrid [Madrid] (UCM)-Consejo Superior de Investigaciones Científicas [Spain] (CSIC), Université Catholique de Louvain (UCL), Institut de Recherche pour le Développement (IRD)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Muséum national d'Histoire naturelle (MNHN)-Institut de Recherche pour le Développement (IRD)-Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Pierre et Marie Curie - Paris 6 (UPMC)-Muséum national d'Histoire naturelle (MNHN), Department of Global Ecology [Carnegie Institution], Consejo Superior de Investigaciones Científicas [Spain] (CSIC)-Universidad Complutense de Madrid [Madrid] (UCM), Environmental Sciences, Sub Gen. Pharmacoepi and Clinical Pharm, and SGPL Stadsgeografie

Subjects
Paleoclimate, 530 Physics, Natural forcing, Settore GEO/12 - Oceanografia e Fisica dell'Atmosfera, 610 Medicine & health, natural forcing, [SDU.STU.CL]Sciences of the Universe [physics]/Earth Sciences/Climatology, last millennium, 550 Earth sciences & geology, Climate and Earth system modelling, CMIP6, PMIP, Last millennium, CISM [CECI], MIP6, PMIP4
Abstract

The pre-industrial millennium is among the periods selected by the Paleoclimate Model Intercomparison Project (PMIP) for experiments contributing to the sixth phase of the Coupled Model Intercomparison Project (CMIP6) and the fourth phase of the PMIP (PMIP4). The past1000 transient simulations serve to investigate the response to (mainly) natural forcing under background conditions not too different from today, and to discriminate between forced and internally generated variability on interannual to centennial timescales. This paper describes the motivation and the experimental set-ups for the PMIP4-CMIP6 past1000 simulations, and discusses the forcing agents orbital, solar, volcanic, and land use/land cover changes, and variations in greenhouse gas concentrations. The past1000 simulations covering the pre-industrial millennium from 850 Common Era (CE) to 1849 CE have to be complemented by historical simulations (1850 to 2014 CE) following the CMIP6 protocol. The external forcings for the past1000 experiments have been adapted to provide a seamless transition across these time periods. Protocols for the past1000 simulations have been divided into three tiers. A default forcing data set has been defined for the Tier 1 (the CMIP6 past1000) experiment. However, the PMIP community has maintained the flexibility to conduct coordinated sensitivity experiments to explore uncertainty in forcing reconstructions as well as parameter uncertainty in dedicated Tier 2 simulations. Additional experiments (Tier 3) are defined to foster collaborative model experiments focusing on the early instrumental period and to extend the temporal range and the scope of the simulations. This paper outlines current and future research foci and common analyses for collaborative work between the PMIP and the observational communities (reconstructions, instrumental data)., Geoscientific Model Development, 10 (11), ISSN:1991-9603, ISSN:1991-959X

Published
2017

41. The PMIP4 contribution to CMIP6 - Part 3: The last millennium, scientific objective, and experimental design for the PMIP4 past1000 simulations

Author

Environmental Sciences, Sub Gen. Pharmacoepi and Clinical Pharm, SGPL Stadsgeografie, Jungclaus, J. H., Bard, E., Baroni, M., Braconnot, P., Cao, J., Chini, L. P., Egorova, T., Evans, M., González-Rouco, J. F., Goosse, H., Hurtt, G. C., Joos, F., Kaplan, J. O., Khodri, M., Klein Goldewijk, K., Krivova, N., LeGrande, A. N., Lorenz, S. J., Luterbacher, J., Man, W., Maycock, Amanda C., Meinshausen, M., Moberg, A., Muscheler, Raimund, Nehrbass-Ahles, C., Otto-Bliesner, B. I., Phipps, S. J., Pongratz, J., Rozanov, E., Schmidt, G. A., Schmidt, H., Schmutz, W., Schurer, A., Shapiro, A. I., Sigl, M., Smerdon, J. E., Solanki, S. K., Timmreck, C., Toohey, M., Usoskin, I. G., Wagner, S., Wu, C.-Y., Yeo, K. L., Zanchettin, D., Zhang, Q., Zorita, E., Environmental Sciences, Sub Gen. Pharmacoepi and Clinical Pharm, SGPL Stadsgeografie, Jungclaus, J. H., Bard, E., Baroni, M., Braconnot, P., Cao, J., Chini, L. P., Egorova, T., Evans, M., González-Rouco, J. F., Goosse, H., Hurtt, G. C., Joos, F., Kaplan, J. O., Khodri, M., Klein Goldewijk, K., Krivova, N., LeGrande, A. N., Lorenz, S. J., Luterbacher, J., Man, W., Maycock, Amanda C., Meinshausen, M., Moberg, A., Muscheler, Raimund, Nehrbass-Ahles, C., Otto-Bliesner, B. I., Phipps, S. J., Pongratz, J., Rozanov, E., Schmidt, G. A., Schmidt, H., Schmutz, W., Schurer, A., Shapiro, A. I., Sigl, M., Smerdon, J. E., Solanki, S. K., Timmreck, C., Toohey, M., Usoskin, I. G., Wagner, S., Wu, C.-Y., Yeo, K. L., Zanchettin, D., Zhang, Q., and Zorita, E.

Published
2017

42. Data Descriptor: A global multiproxy database for temperature reconstructions of the Common Era

Author

Emile-Geay, J, McKay, NP, Kaufman, DS, von Gunten, L, Wang, J, Anchukaitis, KJ, Abram, NJ, Addison, JA, Curran, MAJ, Evans, MN, Henley, BJ, Hao, Z, Martrat, B, McGregor, HV, Neukom, R, Pederson, GT, Stenni, B, Thirumalai, K, Werner, JP, Xu, C, Divine, DV, Dixon, BC, Gergis, J, Mundo, IA, Nakatsuka, T, Phipps, SJ, Routson, CC, Steig, EJ, Tierney, JE, Tyler, JJ, Allen, KJ, Bertler, NAN, Bjorklund, J, Chase, BM, Chen, M-T, Cook, E, de Jong, R, DeLong, KL, Dixon, DA, Ekaykin, AA, Ersek, V, Filipsson, HL, Francus, P, Freund, MB, Frezzotti, M, Gaire, NP, Gajewski, K, Ge, Q, Goosse, H, Gornostaeva, A, Grosjean, M, Horiuchi, K, Hormes, A, Husum, K, Isaksson, E, Kandasamy, S, Kawamura, K, Kilbourne, KH, Koc, N, Leduc, G, Linderholm, HW, Lorrey, AM, Mikhalenko, V, Mortyn, PG, Motoyama, H, Moy, AD, Mulvaney, R, Munz, PM, Nash, DJ, Oerter, H, Opel, T, Orsi, AJ, Ovchinnikov, DV, Porter, TJ, Roop, HA, Saenger, C, Sano, M, Sauchyn, D, Saunders, KM, Seidenkrantz, M-S, Severi, M, Shao, X, Sicre, M-A, Sigl, M, Sinclair, K, St George, S, St Jacques, J-M, Thamban, M, Thapa, UK, Thomas, ER, Turney, C, Uemura, R, Viau, AE, Vladimirova, DO, Wahl, ER, White, JWC, Yu, Z, Zinke, J, Emile-Geay, J, McKay, NP, Kaufman, DS, von Gunten, L, Wang, J, Anchukaitis, KJ, Abram, NJ, Addison, JA, Curran, MAJ, Evans, MN, Henley, BJ, Hao, Z, Martrat, B, McGregor, HV, Neukom, R, Pederson, GT, Stenni, B, Thirumalai, K, Werner, JP, Xu, C, Divine, DV, Dixon, BC, Gergis, J, Mundo, IA, Nakatsuka, T, Phipps, SJ, Routson, CC, Steig, EJ, Tierney, JE, Tyler, JJ, Allen, KJ, Bertler, NAN, Bjorklund, J, Chase, BM, Chen, M-T, Cook, E, de Jong, R, DeLong, KL, Dixon, DA, Ekaykin, AA, Ersek, V, Filipsson, HL, Francus, P, Freund, MB, Frezzotti, M, Gaire, NP, Gajewski, K, Ge, Q, Goosse, H, Gornostaeva, A, Grosjean, M, Horiuchi, K, Hormes, A, Husum, K, Isaksson, E, Kandasamy, S, Kawamura, K, Kilbourne, KH, Koc, N, Leduc, G, Linderholm, HW, Lorrey, AM, Mikhalenko, V, Mortyn, PG, Motoyama, H, Moy, AD, Mulvaney, R, Munz, PM, Nash, DJ, Oerter, H, Opel, T, Orsi, AJ, Ovchinnikov, DV, Porter, TJ, Roop, HA, Saenger, C, Sano, M, Sauchyn, D, Saunders, KM, Seidenkrantz, M-S, Severi, M, Shao, X, Sicre, M-A, Sigl, M, Sinclair, K, St George, S, St Jacques, J-M, Thamban, M, Thapa, UK, Thomas, ER, Turney, C, Uemura, R, Viau, AE, Vladimirova, DO, Wahl, ER, White, JWC, Yu, Z, and Zinke, J

Abstract

Reproducible climate reconstructions of the Common Era (1 CE to present) are key to placing industrial-era warming into the context of natural climatic variability. Here we present a community-sourced database of temperature-sensitive proxy records from the PAGES2k initiative. The database gathers 692 records from 648 locations, including all continental regions and major ocean basins. The records are from trees, ice, sediment, corals, speleothems, documentary evidence, and other archives. They range in length from 50 to 2000 years, with a median of 547 years, while temporal resolution ranges from biweekly to centennial. Nearly half of the proxy time series are significantly correlated with HadCRUT4.2 surface temperature over the period 1850-2014. Global temperature composites show a remarkable degree of coherence between high- and low-resolution archives, with broadly similar patterns across archive types, terrestrial versus marine locations, and screening criteria. The database is suited to investigations of global and regional temperature variability over the Common Era, and is shared in the Linked Paleo Data (LiPD) format, including serializations in Matlab, R and Python.

Published
2017

43. The PMIP4 contribution to CMIP6 – Part 3:the last millennium, scientific objective, and experimental design for the PMIP4 past1000 simulations

Author

Jungclaus, J. H. (Johann H.), Bard, E. (Edouard), Baroni, M. (Melanie), Braconnot, P. (Pascale), Cao, J. (Jian), Chini, L. P. (Louise P.), Egorova, T. (Tania), Evans, M. (Michael), Fidel Gonzalez-Rouco, J. (J.), Goosse, H. (Hugues), Hurtt, G. C. (George C.), Joos, F. (Fortunat), Kaplan, J. O. (Jed O.), Khodri, M. (Myriam), Goldewijk, K. K. (Kees Klein), Krivova, N. (Natalie), LeGrande, A. N. (Allegra N.), Lorenz, S. J. (Stephan J.), Luterbacher, J. (Juerg), Man, W. (Wenmin), Maycock, A. C. (Amanda C.), Meinshausen, M. (Malte), Moberg, A. (Anders), Muscheler, R. (Raimund), Nehrbass-Ahles, C. (Christoph), Otto-Bliesner, B. I. (Bette I.), Phipps, S. J. (Steven J.), Pongratz, J. (Julia), Rozanov, E. (Eugene), Schmidt, G. A. (Gavin A.), Schmidt, H. (Hauke), Schmutz, W. (Werner), Schurer, A. (Andrew), Shapiro, A. I. (Alexander I.), Sigl, M. (Michael), Smerdon, J. E. (Jason E.), Solanki, S. K. (Sami K.), Timmreck, C. (Claudia), Toohey, M. (Matthew), Usoskin, I. G. (Ilya G.), Wagner, S. (Sebastian), Wu, C.-J. (Chi-Ju), Yeo, K. L. (Kok Leng), Zanchettin, D. (Davide), Zhang, Q. (Qiong), Zorita, E. (Eduardo), Jungclaus, J. H. (Johann H.), Bard, E. (Edouard), Baroni, M. (Melanie), Braconnot, P. (Pascale), Cao, J. (Jian), Chini, L. P. (Louise P.), Egorova, T. (Tania), Evans, M. (Michael), Fidel Gonzalez-Rouco, J. (J.), Goosse, H. (Hugues), Hurtt, G. C. (George C.), Joos, F. (Fortunat), Kaplan, J. O. (Jed O.), Khodri, M. (Myriam), Goldewijk, K. K. (Kees Klein), Krivova, N. (Natalie), LeGrande, A. N. (Allegra N.), Lorenz, S. J. (Stephan J.), Luterbacher, J. (Juerg), Man, W. (Wenmin), Maycock, A. C. (Amanda C.), Meinshausen, M. (Malte), Moberg, A. (Anders), Muscheler, R. (Raimund), Nehrbass-Ahles, C. (Christoph), Otto-Bliesner, B. I. (Bette I.), Phipps, S. J. (Steven J.), Pongratz, J. (Julia), Rozanov, E. (Eugene), Schmidt, G. A. (Gavin A.), Schmidt, H. (Hauke), Schmutz, W. (Werner), Schurer, A. (Andrew), Shapiro, A. I. (Alexander I.), Sigl, M. (Michael), Smerdon, J. E. (Jason E.), Solanki, S. K. (Sami K.), Timmreck, C. (Claudia), Toohey, M. (Matthew), Usoskin, I. G. (Ilya G.), Wagner, S. (Sebastian), Wu, C.-J. (Chi-Ju), Yeo, K. L. (Kok Leng), Zanchettin, D. (Davide), Zhang, Q. (Qiong), and Zorita, E. (Eduardo)

Abstract

The pre-industrial millennium is among the periods selected by the Paleoclimate Model Intercomparison Project (PMIP) for experiments contributing to the sixth phase of the Coupled Model Intercomparison Project (CMIP6) and the fourth phase of the PMIP (PMIP4). The past1000 transient simulations serve to investigate the response to (mainly) natural forcing under background conditions not too different from today, and to discriminate between forced and internally generated variability on interannual to centennial timescales. This paper describes the motivation and the experimental set-ups for the PMIP4-CMIP6 past1000 simulations, and discusses the forcing agents orbital, solar, volcanic, and land use/land cover changes, and variations in greenhouse gas concentrations. The past1000 simulations covering the pre-industrial millennium from 850 Common Era (CE) to 1849 CE have to be complemented by historical simulations (1850 to 2014 CE) following the CMIP6 protocol. The external forcings for the past1000 experiments have been adapted to provide a seamless transition across these time periods. Protocols for the past1000 simulations have been divided into three tiers. A default forcing data set has been defined for the Tier 1 (the CMIP6 past1000) experiment. However, the PMIP community has maintained the flexibility to conduct coordinated sensitivity experiments to explore uncertainty in forcing reconstructions as well as parameter uncertainty in dedicated Tier 2 simulations. Additional experiments (Tier 3) are defined to foster collaborative model experiments focusing on the early instrumental period and to extend the temporal range and the scope of the simulations. This paper outlines current and future research foci and common analyses for collaborative work between the PMIP and the observational communities (reconstructions, instrumental data).

Published
2017

44. A global multiproxy database for temperature reconstructions of the Common Era

Author

Emile-Geay, J., McKay, N., Kaufman, D., Von Gunten, L., Wang, J., Anchukaitis, K., Abram, N., Addison, J., Curran, M., Evans, M., Henley, B., Hao, Z., Martrat, B., McGregor, H., Neukom, R., Pederson, G., Stenni, B., Thirumalai, K., Werner, J., Xu, C., Divine, D., Dixon, B., Gergis, J., Mundo, I., Nakatsuka, T., Phipps, S., Routson, C., Steig, E., Tierney, J., Tyler, J., Allen, K., Bertler, N., Björklund, J., Chase, B., Chen, M., Cook, E., De Jong, R., DeLong, K., Dixon, D., Ekaykin, A., Ersek, V., Filipsson, H., Francus, P., Freund, M., Frezzotti, M., Gaire, N., Gajewski, K., Ge, Q., Goosse, H., Gornostaeva, A., Grosjean, M., Horiuchi, K., Hormes, A., Husum, K., Isaksson, E., Kandasamy, S., Kawamura, K., Kilbourne, K., Koç, N., Leduc, G., Linderholm, H., Lorrey, A., Mikhalenko, V., Mortyn, P., Motoyama, H., Moy, A., Mulvaney, R., Munz, P., Nash, D., Oerter, H., Opel, T., Orsi, A., Ovchinnikov, D., Porter, T., Roop, H., Saenger, C., Sano, M., Sauchyn, D., Saunders, K., Seidenkrantz, M., Severi, M., Shao, X., Sicre, M., Sigl, M., Sinclair, K., St George, S., St Jacques, J., Thamban, M., Thapa, U., Thomas, E., Turney, C., Uemura, R., Viau, A., Vladimirova, D., Wahl, E., White, J., Yu, Z., Zinke, Jens, Emile-Geay, J., McKay, N., Kaufman, D., Von Gunten, L., Wang, J., Anchukaitis, K., Abram, N., Addison, J., Curran, M., Evans, M., Henley, B., Hao, Z., Martrat, B., McGregor, H., Neukom, R., Pederson, G., Stenni, B., Thirumalai, K., Werner, J., Xu, C., Divine, D., Dixon, B., Gergis, J., Mundo, I., Nakatsuka, T., Phipps, S., Routson, C., Steig, E., Tierney, J., Tyler, J., Allen, K., Bertler, N., Björklund, J., Chase, B., Chen, M., Cook, E., De Jong, R., DeLong, K., Dixon, D., Ekaykin, A., Ersek, V., Filipsson, H., Francus, P., Freund, M., Frezzotti, M., Gaire, N., Gajewski, K., Ge, Q., Goosse, H., Gornostaeva, A., Grosjean, M., Horiuchi, K., Hormes, A., Husum, K., Isaksson, E., Kandasamy, S., Kawamura, K., Kilbourne, K., Koç, N., Leduc, G., Linderholm, H., Lorrey, A., Mikhalenko, V., Mortyn, P., Motoyama, H., Moy, A., Mulvaney, R., Munz, P., Nash, D., Oerter, H., Opel, T., Orsi, A., Ovchinnikov, D., Porter, T., Roop, H., Saenger, C., Sano, M., Sauchyn, D., Saunders, K., Seidenkrantz, M., Severi, M., Shao, X., Sicre, M., Sigl, M., Sinclair, K., St George, S., St Jacques, J., Thamban, M., Thapa, U., Thomas, E., Turney, C., Uemura, R., Viau, A., Vladimirova, D., Wahl, E., White, J., Yu, Z., and Zinke, Jens

Abstract

Reproducible climate reconstructions of the Common Era (1 CE to present) are key to placing industrial-era warming into the context of natural climatic variability. Here we present a community-sourced database of temperature-sensitive proxy records from the PAGES2k initiative. The database gathers 692 records from 648 locations, including all continental regions and major ocean basins. The records are from trees, ice, sediment, corals, speleothems, documentary evidence, and other archives. They range in length from 50 to 2000 years, with a median of 547 years, while temporal resolution ranges from biweekly to centennial. Nearly half of the proxy time series are significantly correlated with HadCRUT4.2 surface temperature over the period 1850-2014. Global temperature composites show a remarkable degree of coherence between high- and low-resolution archives, with broadly similar patterns across archive types, terrestrial versus marine locations, and screening criteria. The database is suited to investigations of global and regional temperature variability over the Common Era, and is shared in the Linked Paleo Data (LiPD) format, including serializations in Matlab, R and Python.

Published
2017

48. Greenland precipitation trends in a long-term instrumental climate context (1890-2012): evaluation of coastal and ice core records

Author

Mernild, S. H., Hanna, E., Mcconnell, J. R., Sigl, M., Beckerman, A. P., Yde, J. C., Cappelen, J., Malmros, J. K., and Steffen, K.

Subjects
F330 Environmental Physics
Abstract

Here, we present an analysis of monthly, seasonal, and annual long-term precipitation time-series compiled from coastal meteorological stations in Greenland and Greenland Ice Sheet (GrIS) ice cores (including three new ice core records from ACT11D, Tunu2013, and Summit2010). The dataset covers the period from 1890 to 2012, a period of climate warming. For approximately the first decade of the new millennium (2001-2012) minimum and maximum mean annual precipitation conditions are found in Northeast Greenland (Tunu2013 c. 120mm water equivalent (w.e.) year-1) and South Greenland (Ikerasassuaq: c. 2300mm w.e. year-1), respectively. The coastal meteorological stations showed on average increasing trends for 1890-2012 (3.5mm w.e. year-2) and 1961-2012 (1.3mm w.e. year-2). Years with high coastal annual precipitation also had a: (1) significant high number of precipitation days (r2 = 0.59); and (2) high precipitation intensity measured as 24-h precipitation (r2 = 0.54). For the GrIS the precipitation estimated from ice cores increased on average by 0.1mm w.e. year-2 (1890-2000), showing an antiphase variability in precipitation trends between the GrIS and the coastal regions. Around 1960 a major shift occurred in the precipitation pattern towards wetter precipitation conditions for coastal Greenland, while drier conditions became more prevalent on the GrIS. Differences in precipitation trends indicate a heterogeneous spatial distribution of precipitation in Greenland. An Empirical Orthogonal Function analysis reveals a spatiotemporal cycle of precipitation that is linked instantaneously to the North Atlantic Oscillation and the Atlantic Multidecadal Oscillation and with an �6 years lag time response to the Greenland Blocking Index. © 2014 Royal Meteorological Society.

Published
2015

49. Aromatic acids in a Eurasian Arctic ice core: a 3000-year proxy record of biomass burning

Author

Grieman, M. M., Aydin, Murat, Fritzsche, Diedrich, McConnell, J. R., Opel, Thomas, Sigl, M., Saltzman, E.S., Grieman, M. M., Aydin, Murat, Fritzsche, Diedrich, McConnell, J. R., Opel, Thomas, Sigl, M., and Saltzman, E.S.

Abstract

Wildfires and their emissions have significant impacts on ecosystems, climate, atmospheric chemistry and carbon cycling. Well-dated proxy records are needed to study the long-term climatic controls on biomass burning and the associated climate feedbacks. There is a particular lack of information about long-term biomass burning variations in Siberia, the largest forested area in the Northern Hemisphere. In this study we report analyses of aromatic acids (vanillic and para-hydroxybenzoic acids) over the past 3145 years in the Eurasian Arctic Akademii Nauk ice core. These compounds are aerosol-borne, semi-volatile organic compounds derived from lignin combustion. The analyses were made using ion chromatography with electrospray mass spectrometric detection. The levels of these aromatic acids ranged from below the detection limit (.01 to .05 ppb) to about 1 ppb, with roughly 30 % of the samples above the detection limit. In the preindustrial late Holocene, highly elevated aromatic acid levels are observed during four distinct periods (1180–660 BCE, 180–220 CE, 380–660 CE, and 1460–1660 CE). The timing of these periods coincides with the episodic pulsing of ice-rafted debris in the North Atlantic known as Bond events. Aromatic acid levels also are elevated during the onset of the industrial period from 1780 to 1860 CE, but with a different ratio of vanillic and para-hydroxybenzoic acid than is observed during the preindustrial period. This study provides the first millennial scale record of aromatic acids. It clearly demonstrates that coherent aromatic acid signals are recorded in polar ice cores that can be used as proxies for past trends in biomass burning.

Published
2016

50. A Method for Continuous 239Pu Determinations in Arctic and Antarctic Ice Cores

Author

Arienzo, Monica, McConnell, J.R., Chellman, N., Criscitiello, A.S., Curran, M., Fritzsche, Diedrich, Kipfstuhl, Sepp, Mulvaney, R., Nolan, M., Opel, Thomas, Sigl, M., Steffensen, J. P., Arienzo, Monica, McConnell, J.R., Chellman, N., Criscitiello, A.S., Curran, M., Fritzsche, Diedrich, Kipfstuhl, Sepp, Mulvaney, R., Nolan, M., Opel, Thomas, Sigl, M., and Steffensen, J. P.

Abstract

Atmospheric nuclear weapons testing (NWT) resulted in the injection of plutonium (Pu) into the atmosphere and subsequent global deposition. We present a new method for continuous semiquantitative measurement of 239Pu in ice cores, which was used to develop annual records of fallout from NWT in ten ice cores from Greenland and Antarctica. The 239Pu was measured directly using an inductively coupled plasma-sector field mass spectrometer, thereby reducing analysis time and increasing depth-resolution with respect to previous methods. To validate this method, we compared our one year averaged results to published 239Pu records and other records of NWT. The 239Pu profiles from the Arctic ice cores reflected global trends in NWT and were in agreement with discrete Pu profiles from lower latitude ice cores. The 239Pu measurements in the Antarctic ice cores tracked low latitude NWT, consistent with previously published discrete records from Antarctica. Advantages of the continuous 239Pu measurement method are (1) reduced sample preparation and analysis time; (2) no requirement for additional ice samples for NWT fallout determinations; (3) measurements are exactly coregistered with all other chemical, elemental, isotopic, and gas measurements from the continuous analytical system; and (4) the long half-life means the 239Pu record is stable through time.

Published
2016

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