The Winners of the Blue Planet Prize2005

2005
Blue Planet Prize
Professor Sir Nicholas
Shackleton (U.K.)

Dr. Gordon Hisashi Sato
(U.S.A.)

Emeritus Professor, Department of Earth
Sciences, University of Cambridge
Former Head of Godwin Laboratory for
Quaternary Research

Director Emeritus, W. Alton Jones Cell Science
Center, Inc.
Chairman of the Board, A&G Pharmaceutical, Inc.
President, Manzanar Project Corporation

The Sign:
The earth is engraved with thewisdom of nature, leaving its
impression in the changes of theweather, and in the behavior ofanimals giving them life.
Humans have forgotten to listen
to the suffering earth, or to
notice the state of living creatures. The 2005 opening film
touched on the signs in theearth’s history that pointed
towards the future and the creatures that live there.

193

Their Imperial Highnesses Prince
and Princess Akishino congratulate
the laureates at the Congratulatory
Party
His Imperial Highness Prince Akishino congratulates
the laureates

The prizewinners receive their trophies from Chairman Seya

Dr. Jiro Kondo,
chairman of the
Presentation
Committee makes a
toast at theCongratulatory Party

Dr. Gordon Hisashi Sato

Prof. Sir Nicholas Shackleton

J. Thomas Schieffer, Ambassador of the UnitedStates of America to Japan and Graham Fry,
Ambassador of the United Kingdom to Japan,
congratulate the laureates

194

Blue Planet Prize Commemorative Lectures

Profile

Professor Sir Nicholas Shackleton
Emeritus Professor, Department of Earth Sciences, University of Cambridge
Former Head of Godwin Laboratory for Quaternary Research

Education and Academic and Professional Activities
1937
Born on June 23, in London
1961
B.A. University of Cambridge
1965-1972 Senior Assistant in Research, University of Cambridge
1967
Ph.D., University of Cambridge
1972-1987 Assistant Director of Research, Sub-department of Quaternary Research,
Cambridge
1974-1975 Senior Visiting Research Fellow, Lamont-Doherty Geological Observatory,
Columbia University
1975-2004 Senior Research Associate, Lamont-Doherty
1985
Fellow of The Royal Society
1987-1991 Reader, University of Cambridge
1988-1994 Director, Sub-department of Quaternary Research, Cambridge
1990
Fellow, American Geophysical Union
1991-2004 Ad hominem Professor, University of Cambridge
1995
Crafoord Prize, Royal Swedish Academy of Science
1995-2004 Director, Godwin Institute of Quaternary Research, Cambridge
1998
Knighthood (for services to the Earth Science)
2000
Foreign Associate, US National Academy of Sciences
2002
Ewing Medal, American Geophysical Union
2003
Urey Medal, European Association of Geochemistry
2003
Royal Medal (Royal Society of London)
2004
Vetlesen Prize, Columbia University
2004
Emeritus Professor, University of Cambridge
2005
Founder's Medal, Royal Geographical Society
2006
Deceased, January 24

It is important to know and understand climatic change over the past in order to simulate futureclimate change more reliably.
After graduating from Cambridge University with a B.A. in physics, Professor
Shackleton received a Ph.D. with a thesis titled "The Measurement of Palaeotemperatures in
the Quaternary Era" in 1967, and focused his attention on the geologically most recent period195

in the earth's history, the Quaternary which covers about the last 1.8 million years.
During the ice age when ice sheets up to 3 km thick covered North America andScandinavia, lighter oxygen isotope 16O was trapped in the ice sheets and the remaining ocean
water have been enriched in 18O by a measurable amount. He developed a high-resolution
analysis method for oxygen isotope ratios in the tiny fossil shells of foraminifera from theoceans globally and devised a method to analyse more accurately the fluctuations in size of ice
sheets which developed many times during the period, and made contributions to palaeoclimatology.
In 1973, he analysed a core from the western tropical Pacific that contained evidence ofthe most recent reversal of the Earth's magnetic field that occurred about 780,000 years ago. It
was obvious that the ice-volume cycles that he reconstructed occurred roughly every 100,000
years, and he established a method for assigning an age scale for a core, based on the 100,000year cycles from the core.
Further work on the cyclicity in the sediment cores revealed that the major cyclice wasin sync with the major changes in the eccentricity of the earth's orbit, and a paper was published in 1976 together with Drs. J. D. Hays and J. Imbrie, which validated the "Milankovitch
hypothesis" that hypothesized the idea that cyclical changes in the three elements, earth orbit
eccentricity, angle of its rotational axis (obliquity) and precessional changes, caused the glaciation that had occurred during that time.
In the 1990s, after French and Swiss scientists measured the carbon dioxide in air bubbles trapped in ice from the Vostok ice core in central Antarctica and revealed the atmosphericcarbon dioxide concentration for the last 420,000 years, he used the carbon isotope ratios infossil foraminifera to reconstruct past carbon dioxide concentrations. His reconstruction was
surprisingly similar to the first record obtained by French and Swiss scientists. In a later study
he showed that carbon dioxide was a major contributor to past global climate change during
the period and that in fact the main features of climatic variability over the past million years
can be explained taking account of earth's orbital changes as well as natural carbon dioxidechanges.
Recently he worked on the detailed record of the last glacial cycle. He showed that adrastic warming and cooling, such as, temperature difference of 10 degree within 30 years
which the earth had experienced known from the study of ice cores from Greenland can also
be found in sediment cores from the North Atlantic.
Professor Shackleton had major influence on the development of Palaeoceanography
and Palaeoclimatology, and served central roles in several international research projects. He
published more than 200 papers including highly renowned ones, taught and brought up many
young researchers, and was major thrust in these field with his highly positive attitude. Besides
serving as Director of the Godwin Institute for Quaternary Research, he served many key positions such as the President of the International Union for Quaternary Research.
Professor Shackleton had an idea that by knowing the past global climate and eventually the earth's environment through the research in geology, this would enable us to find a way
to tackle the issue of global environmental change in the future, and thus contribute to society.
He poured in his enthusiasm into understanding global climate change during the Quaternary

196

which was also considered as the human era, and he sounded a warning that we should beaware that increase in global warming gas may possibly trigger a rapid climate change that had
happened in the past again in the future, and urged that the human race must make efforts tocontrol the release of greenhouse gases.
Professor Sir Nicholas Shackleton passed away on 24 January, 2006. May he rest inpeace.

197

Lecture

Geological Deposits, Geological Timeand Natural Changes in Climate
Professor Sir Nicholas Shackleton
What are geological deposits?
A geologist who is examining material hundreds of millions of years old with the aid of a geological hammer, might use the expression 'geological deposits' as synonymous with 'rocks'.
However as one becomes interested in younger material one has to consider deposits whichhave not yet experienced sufficient time, pressure and temperature to be converted to rocks. In
addition, one can consider deposits such as the ice in the Greenland ice cap that remains a geological deposit until such time as it melts. In my interpretation, even the bubbles of air that aretrapped in this ice constitute geological deposits. The annually ringed trunk of an ancient tree
may be thought of as a geological deposit, whether or not the tree is living today.
Two very important descriptors of a geological deposit are accumulation rate and time
resolution. On a cut cross-section of a tree, one can see every yearly increment so the resolution is described as annual. The accumulation rate, or radial growth rate, may be of the order
1mm/year. In reality it may be possible to distinguish spring growth from summer growth but
it is not possible to extract monthly information. On the other hand, a mollusc might accumulate a similar thickness per year but might preserve a weekly resolution provided a suitablesampling method is used. On the other hand a muddy, estuarine sediment might accumulate ata similar rate but might only offer a resolution of a hundred to a thousand years due to the prevailing mixing by burrowing organisms on the sea floor (bioturbation) and mixing by bottom
currents.
If funding and time permits, I believe that a scientist should sample a geological section
at close enough depth intervals to achieve the temporal resolution required for his/her project,
or as close as the resolution of the deposits allows, whichever is the smaller. People often ask
me what are the secrets of my success, and I believe one of them is that I have always preferred
to sample as closely as circumstances permit. In contrast, many of my friends would prefer tosample as long a record as possible, sacrificing resolution. It could be argued that the benefitof my approach is purely aesthetic; the closely-sampled record looks nicer. But undoubtedly
the densely sampled record gives the reader greater confidence in the data, because it is easierto see just how reliable the measurements are.
What have I measured? stable isotope ratios
The Chicago scientist Harold Urey was awarded the 1934 Nobel Prize for discovering
Deuterium, the heavier isotope of hydrogen. In 1947 he published a seminal paper1 on fractionation between the stable isotopes of a variety of elements. Here “fractionation” refers to a198

process in which some matter is separated in such a manner that on fraction contains proportionately more of the heavy isotope, while the remainder has proportionately more of the lightisotope. For example, in nature it is observed that when water evaporates the water vapour isdepleted in the heavy isotope of oxygen 18O and the remaining liquid is slightly enriched in 18O.
The reason is that it requires slightly more energy to hold a heavier water molecule in thevapour phase. In his 1947 paper Urey calculated the magnitude of this effect both for the caseof the evaporation of water and for many other phase transitions and chemical reactions. One
example involves the crystallization of calcite (calcium carbonate) from water, and here not
only did Urey calculate the 18O fractionation between the water and the calcite, but he also calculated the effect of temperature on this fractionation. He then suggested that if this fractionation could be measured at different times in the geological past, it would be possible to estimate the palaeotemperature at the time of crystallization.
Together with a team of brilliant colleagues Urey set about developing this idea into a
viable tool. This entailed: 1. developing a sufficiently precise mass spectrometer for measuring the isotope ratios; 2. developing a method for extracting CO2 from carbonate without
introducing additional fractionation; 3. demonstrating that the fractionation exhibited during
calcite crystallization is as predicted by theory; 4. demonstrating that biogenic calcite undergoes the same 18O fractionation during shell growth as does calcite that grows inorganically;and 5. demonstrating that the method does actually give reasonable results for fossils. All thiswas achieved in a remarkable series of papers published in the early 1950’s2.
One additional scientist was needed to set the scene for my entry into the field. Cesare
Emiliani came to Chicago already fortified by a PhD in micropalaeontology (the study of
microscopic fossils) from the University of Bologna in Italy. Using the techniques that Urey’s
team had developed he set out to measure palaeotemperatures in a range of deep-sea sedimentcores and rock outcrops. His outstanding publication (1955)3 was entitled “Pleistocene
Palaeotemperatures”. In this paper Emiliani gave palaeotemperature measurements in coresthat covered over half a million years (as we now know) in cores from the deep Caribbean,equatorial Atlantic, and North Atlantic.
After the second World War Dr (later Sir Harry) Godwin formed a Sub-Department of
Quaternary Research as a small research unit within the Botany School in Cambridge. He wasan all-round botanist and the founder of pollen analysis in Britain. He set up this group because
together with the archaeologist Graeme Clarke he was working on vegetational change in
Britain in relation to the prehistoric humans. Godwin set up the first radiocarbon dating laboratory in Britain in the 1950’s and so was able to put the human and vegetational changes in a
reliable time frame for the first time. About 1960 Dr (later Sir Edward) Bullard suggested that
Godwin should seek funding to set up a laboratory for stable isotope analysis. The idea wasthat in Eastern England marine deposits exist that contain pollen from the nearby land mass aswell as marine fossils; Bullard suggested that the combination of palaeotemperature analysis
using 18O, and pollen analysis would make a unique contribution. Godwin’s grant application
was successful and through a series of random events I was the person who he selected to get
the project under way.
Urey’s team had not been limited as regards sample size because they worked with rel-199

atively large fossils. Emiliani worked with the same equipment – indeed when he moved to apermanent position in the University of Miami he took one of the Chicago mass spectrometerswith him. He was obliged to pick up to 400 foraminifera for each analysis in order to make up
the 5 mg of carbonate that was needed. I soon realised that if I was to set up a successful laboratory without the need to rely on a team of assistants, it would be necessary to have a mass
spectrometer that was about ten times more sensitive than this. The means by which I accomplished this are only of historic interest today4. However it is important to realise that at thetime this was a considerable achievement and for many years my reputation was mainly as “theperson who can analyse 18O in tiny samples of foraminifera.” I had devoted the last year of myundergraduate studies to physics, absolutely essential training given that my first task was torebuild a commercial mass spectrometer such that it could attain the specifications that I
needed. Over the next years I learned a great deal about the disciplines with which I wouldinteract as well as keeping up with Emiliani’s work, and one of the areas that I covered was
glaciology (aided by the existence in Cambridge of the Scott Polar Research Institute). HenceI discovered a fatal weakness in Emiliani’s brilliant papers. Emiliani had appreciated that it wasnecessary to make a correction for changes in the isotopic composition of the ocean when huge
ice sheets accumulated on North America and Fennoscandia. This is because the removal ofisotopically depleted water to form the ice sheets must have left the ocean slightly enriched in18
O. However when I started to calculate this effect more carefully I realized that Emiliani had
seriously underestimated it and indeed that it must have been the dominant cause of the variations in 18O in many of the cores that he analysed5.
At first sight this discovery appeared to weaken the attraction of the field, but I was able
to see it in a different light and to offer two entirely new contributions. First, it would be
extremely valuable to be able to generate a record of global ice volume through time. By
selecting cores from areas where temperature variability might be small, I could optimise thevalue of the measurements from the ice volume point of view. Second, subject to the limitations of each individual core, I could use the 18O record to correlate any core to a master curve.
As it happens the second contribution gained me a large group of high-level colleagues and thisenabled me to achieve the first. John Imbrie, Andrew McIntyre and a number of others had
embarked on an ambitious project named CLIMAP, to generate a map of the surface temperature of the ocean at the time of the last glacial maximum. They had already achieved one taskthat would be needed for this endeavour; they had found a means for mathematically analyzing quantitative faunal data from each sample going down the core so as to estimate a recordof changing sea surface temperature. However they were stymied by the other problem: how
to locate the horizon in each core that corresponded to glacial maximum. When I said that thatwould be easy with my method they were amazed and immediately invited me to joint the
CLIMAP team (which up to that point was an exclusively American venture). The publicationin 1976 of the CLIMAP map of sea-surface temperature during the last ice age maximum 6 washuge accomplishment for the reason (among others) that it provided sufficient data for numerical atmospheric modellers to reconstruct atmospheric circulation in glacial times. One of themany scientists who was stimulated by this opportunity was Syukuro Manabe, winner of thefirst Blue Planet Prize.

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Working with the CLIMAP community, and spending many months in the USA, gaveme access to two incredibly exciting ventures. First, I wanted to analyse a long Pacific core.
My friend Jim Hays taught me to look at deep-sea sediment cores and showed me the coresfrom the East Pacific that he had worked on with Neil Opdyke and others. However the pattern of cyclic carbonate dissolution that he had worked on was a disadvantage from my pointof view, because I wanted to analyse calcite Foraminifera that had not been subject to dissolution on the sea floor. I then turned to the West Pacific and with the assistance of Neil Opdyke
I found what I wanted; a core that appeared uniform from top to bottom. Its reference number
is V28-238; number 238 of the cores collected during the 28th cruise of the Vema. Neil Opdyke
had already located a reversal in the direction of magnetization of the sediment at twelve
metres in the sediment; the last time the direction of the Earth magnetic field reversed wasabout 730 (now known to be 780) thousand years ago. This is known as the BrunhesMatuyama boundary. With Mike Hall to assist me, we worked steadily down the core (MikeHall has worked with me for forty years starting as a junior technician). Each day I plotted themeasurements on graph paper, gluing on extra pieces when necessary. Any suspect measurement I would try to replicate three more times. The excitement was palpable as we saw all thefeatures of the Caribbean records published by Emiliani, and then continued into unknown territory. I could see nothing wrong with the core (Though I looked forward to being the first person to replicate it). I could also see that with the benefit of the Brunhes-Matuyama boundary
fixed at 12 metres in what I called Isotope Stage 19, the time scale that Emiliani has set up,
extrapolating from very shaky dates near the top of his cores, was too short. There were many
important conclusions to be drawn and I wrote what has proved to be a very influential paper7that has been cited well over a thousand times.
Soon after that I saw the opportunity to analyse another long core. An Englishman
named David Parkin had developed a method for estimating changes in the vigour of the windthat blows dust out into the Atlantic Ocean from the Sahara Desert. He had a long record that
included the Brunhes-Matuyama boundary and since the data showed most vigorous winds
near the top of the core he concluded that winds were weaker during glacial times. I persuaded
him to delay publishing his conclusions until I could develop an oxygen isotope record andestablish whether greater wind vigour was consistently associated with lighter 18O values. It
turned out that David Parkin had missed the very short Holocene and that in general more vigorous winds were consistently associated with the glacials. This study8 confirmed the importance of my oxygen isotope stratigraphy; suddenly a method existed by means of which a
record of variations in an important palaeoclimate parameter (in this case, wind) could bedirectly linked to a standard stratigraphy and associated time scale. Soon after this, Neil
Opdyke suggested that I should work on another core V28-239 that extended about two million years into the past. The accumulation rate of this core was lower but by analysing it every
5cm instead of every 10cm I was able to obtain a nice record of the whole Pleistocene9.
When I first showed the data from core V28-238, my colleague John Imbrie immediately wanted to perform a spectral analysis of the data, in order to test the long-standing“Milankovitch Hypothesis”. In the 1920’s Milutin Milankovitch has hypothesised that the ice
ages were caused by changes in the distribution of the sun’s energy over the earth, which in201

turn arise due to changes in the geometry of the earth-sun system. It had never been possible
to test this because continuous records of changing climate were not available until Emiliani
published his 18O records, and because these could not be used because of the lack of age control. We started working of the spectral analysis but then it emerged that Jim Hays was working on cores from the subantarctic Indian Ocean that had several advantages over my core.
Most important, they had twice the accumulation rate of core V28-238. Jim Hays generated
records of sea-surface temperature in the Southern hemisphere, while I generated a Northernhemisphere record from the 18O measurements, since the fluctuating ice sheets accumulated on
the Northern hemisphere continents. We showed10 that the three periodicities with which theorbit changes (100,000 years, 40,000 years and 21,000 years) were all present in the data, justas Milankovitch theory predicted.
We realised while finalising the publication that it was possible to fine-tune the timescale by aligning the cycles in a core with those calculated by astronomical theory, by the early
1980’s we had constructed an astronomically tuned and averaged stable isotope record known
as the SPECMAP stack11, which has been incredibly valuable as a template for workers toplace their data on a highly detailed common time scale. In 1991 I improved this with new data
and was able to show that the age of the Brunhes-Matuyama reversal was 780,000 years rather
than 730,000 years as had been believed12; I also recalibrated several earlier reversals.
Surprisingly, these recalibrations were very soon accepted because new laboratory measurements also suggested that the published ages required correction. I was able to carry the work
further back in time, ultimately calibrating the geological time scale back to about 30 million
years13.
In 1975 I was invited to a meeting in Hawaii concerned with carbon dioxide, and I
decided to think about the isotopes of carbon. Every day that I collected 18O data I also collected 13C data but up to that time I had only used them to make a small correction to the 18O
measurements. The most important process that gives rise to variations in 13C in nature is photosynthesis; plants, and organic matter that derives from them, contain about two percent less13
C than the CO2 from which they grew. When I saw in my collection of 13C data that the ocean
has undergone systematic variations in the 13C content I reasoned that the only plausible explanation had to be was that the mass of organic matter on planet Earth had fluctuated on a glacialinterglacial time scale. Investigating the literature I found that the area that is covered by tropical rainforest was reduced during glacial times because it was drier. At the same time large
areas of terrain that are now vegetated, were then covered by ice sheets. It seemed that I had
stumbled across a method for estimating changes in the mass of organic matter covering thecontinents. When the continental biomass (including soil) diminished, the organic carbon thatwas released must have oxidised and ended up in the ocean14.
Soon after this, two reports appeared claiming that the concentration of carbon dioxidein “fossil” air bubbles from the glacial part of the Antarctic ice sheet is less than that of preindustrial air. Wallace Broecker (another past Blue Planet Prize winner) gave a talk which I
was lucky enough to hear before he published it15. He explained that the only mechanism capable of reducing the carbon dioxide in the atmosphere from 280 to 200 parts per million by volume was one that transferred it to the deep ocean, and he described the working of the “bio-202logical pump” that controls the equilibrium pressure of carbon dioxide over the ocean. In theocean surface layer photosynthesis removes some of the dissolved carbon dioxide by converting it to organic matter, which sinks to the deep ocean and oxidises there. The proportion thatcan be photosynthesised is limited by the concentration of nutrients in the surface water. This
process leads to an enrichment in 13C in the remaining dissolved carbon dioxide that is available for Foraminifera to build their calcite shells with. Meanwhile the rare genera ofForaminifera that live on the sea floor build their shells from average ocean carbon dioxide, sothat the strength of the “biological pump” can be monitored by the 13C difference between theshells of the planktonic (floating near the surface) foraminifera and the benthonic (living on thesea floor) foraminifera. I sought a suitable core and carefully selected benthonic and planktonic specimens to get the best record. Sure enough there was a larger 13C difference between
surface water and bottom water in the glacial part of the core, consistent with the publisheddata from the ice cores that showed a lower carbon dioxide concentration in the air bubbles
from glacial times. I continued and obtained a record that predicted similar values to today inthe last interglacial. My glaciologist friends in France were shocked when they saw this record
published in the journal Nature16 because they had already analysed ice from the Antarctic ice
core at Vostok, and saw at once the similarities between their real carbon dioxide record andmy reconstruction.
I have reviewed for you some of the work I have done which may give you an idea why
I have been selected for this wonderful award. Each publication was based on a lot of new analytical data, and indeed much of my success has depended on the fact that I and my assistantMike Hall have always had the philosophy that to justify the support of my funding agents, thelab ought to be generating data all the time. However five years ago I wrote a paper that contains no new data and instead is based on combining data from my lab with different data published by Robert Petit and his colleagues in the French ice core community. In some ways I
regard it as my best paper17 and of course it is far too complicated to explain to a general audience. Nevertheless I will explain some of its importance. The key was the fact that there is arecord from the Vostok ice core of the changing isotopic composition of the atmospheric oxygen that is trapped in bubbles in the ice. The trapping occurs at the point where that accumulating snow on the ice surface becomes sufficiently packed down that the air can no longer
exchange with the overlying atmosphere (this trapping happens tens of metres below the surface). Now atmospheric oxygen equilibrates with ocean water through global photosynthesis
with many complex steps, but if everything else is assumed not to change, the atmospheric
oxygen would follow changes in the isotopic composition of the ocean with a lag of about athousand years. By comparing this record with the deep-sea oxygen isotope record from carbonate microfossils, I was able to separate the ice-volume component of the many deep-sea
records I had published from the temperature component, something that we have never previously been able to do. Thus I found that the ice volume component does indeed lag (i.e. it
responds with a delay) behind the carbon dioxide record. Some people have argued thatchanges in the ice sheets caused the changes in atmospheric carbon dioxide; I believe thesedata show the reverse; carbon dioxide was a major player in causing the glacial cycles.
Ultimately if we claim to be able to explain past climate, we want to be able to take the203carbon dioxide record and the orbital variations and model the resulting climate record, and tocompare this model result with the geological observations. I believe that at the very simplest
level we can actually do that.
The natural range of variation in atmospheric carbon dioxide during the ice ages, which
had such a dramatic effect on the earth’s climate, was about 80 parts per million by volume.
This range has already been exceeded by the man-made increase over the past century. The
geological record is very important in ramming home the message, that it is imperative that westop the carbon dioxide rise that is causing global warming.
References
1 Urey, H.C. (1947) The thermodynamic properties of isotopic substances. Jour. Chem. Soc. 1947, pp 562-581
2 Epstein, S., Buchsbaum, R., Lowenstam, H.A., & Urey, H.C (1951) Carbonate-water isotopic temperaturescale. Geological Society of America Bulletin, vol 62, pp 417-426
3 Emiliani, C. (1955) Pleistocene temperatures. Journal of Geology, vol 63, pp 538-578
4 Shackleton, N.J. (1965) The high-precision isotopic analysis of oxygen and carbon in carbon dioxide. Journalof Scientific Instruments, vol 42, pp 689-692
5 Shackleton, N.J. (1967) Oxygen isotope analyses and Pleistocene temperatures re-assessed. Nature, vol 215, pp
15-17
6 CLIMAP project members (1976) The surface of the ice-age Earth. Science, vol 191, pp 1131-1137
7 Shackleton, N.J.& Opdyke, N.D. (1973) Oxygen isotope and palaeomagnetic stratigraphy of equatorial Pacificcore V28-238: oxygen isotope temperatures and ice volumes on a 105 year and 106 year scale, Quaternary
Research, vol 3, pp 39-55
8 Parkin, D.W.,& Shackleton, N.J. (1973) Trade wind and temperature correlations down a deep-sea core off the
Saharan coast. Nature, vol 245, pp 455-457
9 Shackleton, N.J.& Opdyke, N.D. (1976) Oxygen isotope and paleomagnetic stratigraphy of Pacific core V28239, Late Pliocene to Latest Pleistocene. Geol. Soc. America Memoir vol 145, pp 449-464.
10 Hays, J.D., Imbrie, J.& Shackleton, N.J. (1976) Variations in the earth's orbit: pacemaker of the ice ages.
Science, vol 194, pp 1121-1131
11 Imbrie, J., Hays, J.D., Martinson, D.G., McIntyre, A., Mix, A., Morley, J.J., Pisias, N.G., Prell, W. &Shackleton, N.J. (1984) The orbital theory of Pleistocene climate: support from a revised chronology of themarine δ18O record In: Berger, A., Imbrie, J., Hays, J., Kukla, G. & Saltzman, B. (eds) Milankovitch andClimate. Hingham, Mass: D. Reidel, pp 269-305
12 Shackleton, N.J., Berger, A. & Peltier, W.R. (1990) An alternative astronomical calibration of the Lower
Pleistocene timescale based on ODP Site 677. Transactions of The Royal Society of Edinburgh: Earth Sciences,
vol 81, pp 251-261
13 Shackleton, N.J., Crowhurst, S.J., Weedon, G.P & Laskar, J. (1999) Astronomical calibration of OligoceneMiocene time, Philosophical Transactions of the Royal Society London, vol 357, pp 1907-1929
14 Shackleton, N.J. (1977) Carbon-13 in Uvigerina: tropical rainforest history and the Equatorial Pacific carbonate dissolution cycles In: N.R. Andersen and A. Malahoff the Fate of Fossil Fuel CO2 in the Oceans. New York,
Plenum Press, pp. 401-427
15 Broecker, W.S. (1982) Glacial to interglacial changes in ocean chemistry. Progr. Oceanogr., vol 11, pp 151-197
16 Shackleton, N.J., Hall, M.A., Line, J. & Cang Shuxi (1983) Carbon isotope data in core V19-30 confirm reduced
carbon dioxide concentration in the ice age atmosphere. Nature, vol 306, pp 319-322
17 Shackleton, N.J. (2000) The 100,000-Year Ice-Age Cycle Identified and Found to Lag Temperature, Carbon
Dioxide, and Orbital Eccentricity. Science, vol 289, pp 1897-1902

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Isotope deviation from laboratory standard(δ18O, 00/00)

Figure 1. Photograph of a limpet from the South African coast, cut in half and sampled with a small drill for oxygen isotope analysis.

+0.5

+0.5

+1.5

EDGE
Figure 2. Oxygen isotope record for shell in Fig. 1, covering two years of growth. This crude sampling is goodenough to determine the season during which prehistoric people were eating shellfish (winter), but it would be technically possible with modern methods to sample at weekly intervals. This is an example of geological measurements on a very fine time scale.

205

Figure 3. The magnetic measurements that were carried out by Neil Opdyke in core V28-238 (upper part of figure) before I sampled the core. It is apparent that the direction of magnetization of the sediment switches by 180
degrees at 12 meters depth in the core. We know that the last time the field was consistently oriented in the reverse
direction was about 780,000 years ago.

SHACKLET ON AND OPDYKE

Figure 4. The oxygen isotope measurements in core V28-238. This figure, published in 1973, demonstrated forthe first time the existence of 100,000-year cyclicity of glaciations over the past million years and has been
described as a “Rosetta Stone” for the ice ages.

206

OXYGEN ISOTOPE RECORD OD LATE OLEISTOCENE

Figure 5. This figure illustrates the effect of sediment accumulation rate on the character of the record obtained byoxygen isotope analysis. At the bottom 100,000 years is compressed into only a meter of sediment and all the finedetail is lost. As the accumulation rate increases in cores toward the top of the figure the last 100,000 years are
revealed in four to ten meters and the important details of the last glacial cycle are reproducibly revealed.

207

ODP Log 154, Site 925

Figure 6. Climate cycles (probably including cyclic appearance and disappearance of the Antarctic ice sheet)between 15 million and 16.6 million years ago are illustrated. Many different climate-sensitive parameters were
measured, and it is apparent that all display approximately the same cyclicity.

208Core V19-30
Atmospheric CO2 from C-13

Figure 7. The top two records in this figure show carbon isotope records from the surface waters, and from thewater bathing the sea floor, in the Eastern equatorial Pacific. The next record shows the carbon isotope gradient
between the surface and deep water as a function of time (obtained by subtracting the second record from the first).
To a first approximation this provides an estimate of changing carbon dioxide in the atmosphere. The bottom
record shows the oxygen isotope record of the core. From this it can be concluded that carbon dioxide was higher
during interglacials and lower during glacials.

209

Figure 8. The top and bottom records on this figure show stable isotope records (roughly proportional to air temperature when the snow was falling) from Greenland ice (measured by Johnsen and co-workers in Copenhagen) andfrom Antarctic ice (measured by Petit and co-workers in Grenoble). The middle two records are stable isotope
records (proxies for water temperature) in surface water and in deep (3000 m) water near Portugal, both measured
in the same samples. All four records are on a consistent age scale covering the interval from 25,000 to 65,000 years
ago during the last ice age. On the scale of rapid events during the last ice age it appears that while the temperatureof the surface of the North Atlantic changed in synchrony with Greenland, the temperature of the deep waters varied in synchrony with the high southern latitudes.

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Figure 9. Each panel includes the same oxygen isotope record from a deep-sea core, superimposed on a model thatpartly simulates the record; each covers 400,000 years. Above each pair is a plot of the residual (obtained by subtracting the model from the data). The upper two panels use different versions of a model using only data for thevariations in the Earth’s orbital parameters and have quite a large-amplitude residual. The model for the lowest
panel incorporates the record of atmospheric carbon dioxide concentration as measured in bubbles from the Vostok
Antarctic ice core (from Petit and colleagues) and has a much smaller residual.

211

Major Publications
Professor Sir Nicholas Shackleton
Publications
Shackleton, N.J. (1965) Some variations in the technique for measuring carbon and oxygen isotope ratios in small
quantities of calcium carbonate. In: Tongiorgi, E. ed. Stable Isotopes in Oceanographic Studies andPaleotemperatures. Pisa: Consiglio Nazionale delle Ricerche, 155-159.
Shackleton, N.J. (1965) The high-precision isotopic analysis of oxygen and carbon in carbon dioxide. Journal of
Scientific Instruments, 42, 689-692.
Shackleton, N.J. (1967) Oxygen isotope analyses and Pleistocene temperatures re-assessed. Nature, 215, 15-17.
Shackleton, N.J. (1967) The measurement of Palaeotemperatures in the Quaternary Era. Ph.D. Thesis, Universityof Cambridge.
Shackleton, N.J. & Turner, C. (1967) Correlation between marine and terrestrial Pleistocene successions. Nature,
216, 1079-1082.
Shackleton, N.J. (1968) Depth of Pelagic Foraminifera and Isotopic Changes in Pleistocene Oceans. Nature, 218,
79-80.
Shackleton, N.J. (1968) The Mollusca, the Crustacea, The Echinodermata. In: Evans, J.D. & Renfrew, C. (Eds.)
Excavations at Saliagos near Antiparos. London: Thames and Hudson, Appendix IX, 122-138.
Shackleton, N.J. (1968) Knossos Marine Mollusca (Neolithic). Annual British School of Archaeology at Athens,63, 264-266.
Shackleton, N.J. (1969) Preliminary observations on the marine shells. In: Jacobsen, T.W. (Ed.) Excavations at
Porto Cheli and vicinity, Preliminary Report. Appendix 1. Hesperia, 38, 379-380.
Shackleton, N.J. (1969) Marine mollusca in archaeology. In: Brothwell, D. & Higgs, E.S. (Eds.) Science in
Archaeology, 2nd ed. London: Thames and Hudson, 407-414.
Shackleton, N.J. (1969) The last interglacial in the marine and terrestrial records. Proceedings of the Royal Society,
B 174, 135-154.
Shackleton, N.J. (1969) World may freeze in new ice age very soon. Geogr. Mag., 41, 705.
Shackleton, N.J. (1969) Palaeotemperatures. McGraw-Hill Yearbook Science and Technology, 251-252. Book
contribution.
Shackleton, N.J. (1970) Stable isotope study of the Palaeoenvironment of Nea Nikomedeia, Greece. Nature, 227,
943-944.
Shackleton, N.J. & Renfrew, C. (1970) Neolithic trade routes re-aligned by oxygen isotope analyses. Nature, 228,1062-1065.
Shackleton, N.J. (1971) Items 367-394. The Phanerozoic Time-scale - a supplement. Special Publication of theGeological Society, No. 5. London. , 80-110.
Shackleton, N.J. (1971) Notes on Pleistocene radiometric age-determinations itemised in this volume. In: Harland,
W.B. & Francis, E.H. (Eds.) The Phanerozoic Time-scale: a supplement. Special Publication of the GeologicalSociety No. 5, London, Part 1, 35-38. Book contribution
Shackleton, N.J. (1972) Late Cenozoic Glacial Ages, edited by Karl K. Turekian. A review. EOS (Transactions of
the American Geophysical Union), 53, 883-884.
Shackleton, N.J. (1972) The Shells: Appendix VII to Myrtos: an early Bronze Age Settlement in Crete British
School at Athens, Supplementary Volume, 7, 321-325.
Shackleton, N.J. (1972) Ocean palaeotemperature changes round Africa. In: Van Zinderen Bakker, E.M. (ed)Palaeoecology of Africa, the surrounding islands and Antarctica. Cape Town: Balkema, VI, 37-38.
Van Donk, J., Saito, T & Shackleton, N.J. (1972) Oxygen isotopic composition of benthonic and planktonic
foraminifera of earliest Pliocene age at Site 132 - Tyrrhenian basin. In Ryan, W.B.F., Hsü, K.J. et al., 1972,
Initial reports of the Deep Sea Drilling Project, Volume XIII, Washington (US Government Printing Office),
XIII, 798-800.
Luz, B. (1973) Stratigraphic and Paleoclimatic analysis of Late Pleistocene tropical southeast Pacific cores (withan Appendix by N.J. Shackleton) Quaternary Research, 3, 56-72.

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Parkin, D.W. & Shackleton, N.J. (1973) Trade wind and temperature correlations down a deep-sea core off the
Saharan coast. Nature, 245, 455-457.
Shackleton, N.J. (1973) Oxygen isotope analysis as a means of determining season of occupation of prehistoric
midden sites. Archaeometry, 15, 133-141.
Shackleton, N.J. & Opdyke, N.D. (1973) Oxygen isotope and paleomagnetic stratigraphy of Equatorial Pacific core
V28-238: oxygen isotope temperatures and ice volumes on a 105 and 106 year scale. Quaternary Research, 3,39-55. reprinted in Benchmark Papers in Geology. Stroudsburg, Pennsylvania: Dowden, Hutchinson & Ross,
Inc., 54, 270-286.
Shackleton, N.J., Wiseman, J.D.H., & Buckley, H.A. (1973) Non-equilibrium isotopic fractionation between seawater and planktonic foraminiferal tests. Nature, 242, 177-179.
Emiliani, C. & Shackleton, N.J. (1974) The Brunhes epoch: isotopic paleotemperatures and geochronology.
Science, 183, 511-514.
Shackleton, N.J. (1974) Attainment of isotopic equilibrium between ocean water and the benthonic foraminifera
genus Uvigerina: isotopic changes in the ocean during the last glacial. Colloques Internationaux du Centre
National du Recherche Scientifique, 219, 203-210.
Shackleton, N.J. (1974) Oxygen isotopic demonstration of winter seasonal occupation. (Contribution to) Resultsof recent investigations at Tamar Hat. Saxon, E.C. (Ed.) Libyca, XXII, 49-91.
Wiseman, J.D.H., Shackleton, N.J. & Buckley, H.A. (1974) Stereoscan and oxygen isotope studies of some Indian
Ocean planktonic foraminifera. I. mar. biol. Ass. India, 16, 759-756.
Kennett, J.-P. & Shackleton, N.J. (1975) Laurentide ice sheet meltwater recorded in Gulf of Mexico deep-sea
cores. Science, 188, 147-150.
Luz, B. & Shackleton, N.J. (1975) CaCO3 solution in the tropical east Pacific during the past 130,000 years.
Cushman Foundation for Foraminiferal Research Special Publication, 13, 142-150.
Ninkovitch, D. & Shackleton, N.J. (1975) Distribution, stratigraphic position and age of ash layer "L", in the
Panama Basin region. Earth and Planetary Science Letters, 27, 20-34.
Shackleton, N.J. (1975) The stratigraphic record of deep-sea cores and its implications for the assessment ofglacials, interglacials, stadials and interstadials in the mid-Pleistocene. In: Butzer, K.W. & Isaac, G.L. (Eds.),
After the Australopithecines, 1-24.
Shackleton, N.J. & Kennett, J.P. (1975) Late Cenozoic oxygen and carbon isotopic changes at DSDP Site 284:
implications for glacial history of the northern hemisphere and Antarctica. In Kennett, J.P., Houtz, R.E., et al.,1975 Initial Reports of the Deep Sea Drilling Project, Volume XXIX, Washington (U.S. Government Printing
Office), 29, 801-807.
Shackleton, N.J. & Kennett, J.P. (1975) Paleotemperature history of the Cenozoic and the initiation of Antarctic
glaciation: oxygen and carbon isotope analyses in DSDP Sites 277, 279 and 281. In Kennett, J.P., Houtz, R.E.
et al, 1975 Initial Reports of the Deep Sea Drilling Project, Volume XXIX, Washington (U.S. Government
Printing Office), 29, 743-755.
CLIMAP project members (inc. Shackleton, N.J.) (1976) The Surface of the Ice-Age Earth. Science, 191, 11311137.
Hays, J.D., Imbrie, J. & Shackleton, N.J. (1976) Variations in the Earth's orbit: Pacemaker of the ice ages. Science,
194, 1121-1132.
Hays, J.D., Lozano, J.A., Shackleton, N.J. & Irving, G. (1976) Reconstruction of the Atlantic and Western Indian
Ocean Sectors of the 18,000 B.P. Antarctic Ocean. Geological Society of America Memoir, 145, 337-371.
Hays, J.D. & Shackleton, N.J. (1976) Globally synchronous extinction of the radiolarian Stylatractus universus.
Geology, 4, 649-652.
Kennett, J.P. & Shackleton, N.J. (1976) Oxygen isotopic evidence for the development of the psychrosphere 38
Myr ago. Nature, 260, 513-515.
Shackleton, N.J & Opdyke, N.D. (1976) Oxygen isotope and paleomagnetic stratigraphy of Pacific core V28-239,
Late Pliocene to Latest Pleistocene. In: Cline, R.M. and Hays, J.D. Investigation of Late Quaternary
Paleoceanography and Paleoclimatology, Geological Society of America Memoir, 145, 449-464. reprinted in
Benchmark Papers in Geology. Stroudsburg, Pennsylvania: Dowden, Hutchinson & Ross, Inc., 54, 287-302.
Boersma, A. & Shackleton, N.J. (1977) Oxygen and carbon isotope record through the Oligocene, DSPD Site 366,
Equatorial Atlantic. In Lancelot, Y., Seibold, E. et al., 1977 Initial Reports of the Deep Sea Drilling Project,
Volume XLI, Washington (U.S. Government Printing Office), 41, 957-962.

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Boersma, A. & Shackleton, N.J. (1977) Tertiary oxygen and carbon isotope stratigraphy, Site 357 (mid latitude
South Atlantic). In Supko, P.R., Perch-Nielsen, K. et al. 1977 Initial Reports of the Deep Sea Drilling Project,
Volume XXXIX, Washington (U.S. Government Printing Office), 39, 911-924.
Hays, J.D., Imbrie, J. & Shackleton, N.J. (1977) Variations in the Earth's orbit: Pacemaker of the ice ages? Science,
198, 529-530.
Peng, T.H., Broecker, W.S., Kipphut, G. & Shackleton, N.J. (1977) Benthic mixing in deep sea cores as determinedby 14C dating and its implications regarding climate stratigraphy and the fate of fossil fuel CO2. In: Andersen,
N.R. & Malahoff, A. (Eds.) The Fate of Fossil Fuel CO2 in the Oceans New York, Plenum Press, pp. 355-373.
Shackleton, N.J. (1977) Carbon-13 in Uvigerina: tropical rainforest history and the Equatorial Pacific carbonate dissolution cycles. In: Andersen, N.R. & Malahoff, A. (Eds.) The Fate of Fossil Fuel CO2 in the Oceans New York,
Plenum Press, pp. 401-427.
Shackleton, N.J. (1977) The oxygen isotope stratigraphic record of the late Pleistocene. In: The Changing
Environmental Conditions in Great Britain and Ireland during the Devensian (last) Cold Stage, a meeting fordiscussion organised by G.F. Mitchell and R.G. West. Phil. Trans. Roy. Soc., B 280, 169-179.
Shackleton, N.J. (1977) Oxygen isotope stratigraphy of the Middle Pleistocene. British Quaternary Studies.
Shotton, F.W. (Ed.) Oxford: Clarendon, 1-16.
Shackleton, N.J. & Matthews, R.K. (1977) Oxygen isotope stratigraphy in Late Pleistocene coral terraces in
Barbados. Nature, 268, 618-619.
Shackleton, N.J. & Opdyke, N.D. (1977) Oxygen isotope and palaeomagnetic evidence for early Northern
Hemisphere glaciation. Nature, 270, 216-219. reprinted in Benchmark Papers in Geology. Stroudsburg,
Pennsylvania: Dowden, Hutchinson & Ross, Inc, 54, 303-306.
Thierstein, H.R., Geitzenauer, K.R., Molfino, B. & Shackleton, N.J. (1977) Global synchroneity of late Quaternary
coccolith datum levels: validation by oxygen isotopes. Geology, 5, 400-404.
Burckle, L.H., Clarke, D.B. & Shackleton, N.J. (1978) Isochronous last-abundant-appearance datum (LAAD) of
the diatom Hemidiscus karstenii in the sub-Antarctic. Geology, 6, 243-246.
Kellogg, T.B., Duplessy, J.-C. & Shackleton, N.J. (1978) Planktonic foraminiferal and oxygen isotopic stratigraphy and paleoclimatology of Norwegian Sea deep-sea cores. Boreas, 7, 61-73.
Kerrich, R., Beckinsale, R.D. & Shackleton, N.J. (1978) The physical and hydrothermal regime of tectonic vein
systems: evidence from stable isotope and fluid inclusion studies. N. Jahrbuch f. Mineralogie. Abhandlungen,131, 225-239.
Ninkovitch, D., Shackleton, N.J., Abdel-Monem, A.A., Obradovich, J.D. & Izett, G. (1978) K-Ar age of the late
Pleistocene eruption of Toba, north Sumatra. Nature, 276, 574-577.
Shackleton, N.J. (1978) Some results of the CLIMAP project. In: Pittock, A.B., Frakes, L.A., Jenssen, D. Petersen,
J.A. & Zillman, J. (Eds.) Climatic change and variability - a Southern Perspective. Cambridge: Cambridge
University Press, 69-76.
Shackleton, N.J. (1978) Evolution of the Earth's climate during the Tertiary era. Evolution of planetary atmospheres and climatology of the Earth. Toulouse, 49-58.
Shackleton, N.J. & Vincent, E. (1978) Oxygen and carbon isotope studies in recent foraminifera from the southwest Indian Ocean. Marine Micropalaeontology, 3, 1-13.
Boersma, A., Shackleton, N.J., Hall, M. & Given, Q. (1979) Carbon and oxygen isotope records at DSDP Site 384(North Atlantic) and some Palaeocene paleotemperatures and carbon isotope variations in the Atlantic Ocean.
In Tucholke, B.E., Vogt, P.R., et al., 1979, Initial Reports of the Deep Sea Drilling Project, v.43: Washington(U.S. Government Printing Office), 43, 695-717.
Heusser, L.E. & Shackleton, N.J. (1979) Direct marine-continental correlation: 150,000-year oxygen isotope.
pollen record from the North Pacific. Science, 204, 837-839.
Jenkins, D.G. & Shackleton, N.J. (1979) Parallel changes in species diversity and palaeotemperature in the Lower
Miocene. Nature, 278, 50-51.
Kennett, J.P., Shackleton, N.J., Margolis, S.V., Goodney, D.E., Dudley, W.C. & Kroopnick, P.M. (1979) Late
Cenozoic oxygen and carbon isotopic history and volcanic ash stratigraphy: DSDP site 284, South Pacific.
American Journal of Science, 279, 52-69.
Morley, J.J. & Shackleton, N.J. (1979) Extension of the radiolarian Stylatractus universus as a biostratigraphic
datum to the Atlantic Ocean. Geology, 6, 309-311.
Shackleton, N.J. & Cita, M.B. (1979) Oxygen and carbon isotope stratigraphy of benthic foraminifers at site 397:

214detailed history of climatic change during the late neogene. In Von Rad, U., Ryan, W.B.F. et al., Initial Reportsof the Deep Sea Drilling Project v.47, Part 1: Washington (US Government Printing Office), XLVII, 433-445.
Streeter, S.S. & Shackleton, N.J. (1979) Paleocirculation of the Deep North Atlantic: 150,000-year record of benthic foraminifera and oxygen-18. Science, 203, 168-171.
Thompson, P.R., Be, A.W.H., Duplessy, J.-C., & Shackleton, N.J. (1979) Disappearance of pink-pigmented
Globigerinoides ruber at 120,000 yr BP in the Indian and Pacific Oceans. Nature, 280, 554-557.
Berggren, W.A., Burckle, L.H., Cita, M.B., Cooke, H.B.S., Funnell, B.M., Gartner, S., Hays, J.D., Kennett, J.P.,
Opdyke, N.D., Pastouret, L., Shackleton, N.J. & Takayanagi, Y. (1980) Towards a Quaternary time scale.
Quaternary Research, 13, 277-302.
Keigwin, L.D. & Shackleton, N.J. (1980) Uppermost Miocene carbon isotope stratigraphy of a piston core in theequatorial Pacific. Nature, 284, 613-614.
Shackleton, N.J. (1980) Deep Drilling in African lakes. Nature, 288, 211-212.
Shackleton, N.J. (1980) Stratigraphy and chronology of the Klassies River Mouth deposits: oxygen isotope evidence. In: Singer, R. & Wymer, J.J. (Eds.) Klassies River Mouth Chicago: The University of Chicago Press,
194-199. Book contribution
Thompson, P.R. & Shackleton, N.J. (1980) North Pacific palaeoceanography: late Quaternary coiling variations ofplanktonic foraminifer Neogloboquadrina pachyderma. Nature, 287, 829-833.
Boersma, A. & Shackleton, N.J. (1981) Oxygen- and carbon-isotope variations and planktonic-foraminifer depth
habitats, late Cretaceous to Paleocene, Central Pacific, Deep Sea Drilling Project Sites 463 and 465. In Thiede,
J. Vallier, T. et al., Init. Repts DSDP, 62: Washington (US Govt. Printing Office), 62, 513-526.
Burckle, L.H., Shackleton, N.J. & Brombie, S.L. (1981) Late Quaternary stratigraphy for the equatorial Pacificbased upon the diatom Coscinodiscus nodulifer. Micropaleontology, 27, 352-355.
CLIMAP project members (1981) Seasonal reconstructions of the Earth's surface at the last glacial maximum. In:
Cline, R. (Ed.) The Geological Society of America. Map and Chart Series, MC-36.
Shackleton, N.J. & Boersma, A. (1981) The climate of the Eocene ocean. Journal of the Geological Society, 138,
153-157.
Shackleton, N.J. (1982) The deep-sea sediment record of climate variability. Prog. Oceanog., 11, 199-218.
Shackleton, N.J. & Hall, M.A. (1982) Oxygen isotope study of continuous scrape samples from site 480. In Curray,
J.R., Moore, D.G. et al., Init. Repts DSDP, 64: Washington (U.S. Govt. Printing Office), 64, 1251-1254.
Backman, J., Shackleton, N.J. & Tauxe, L. (1983) Quantitative nannofossil correlation to open ocean deep-sea sections from Plio-Pleistocene boundary at Vrica, Italy. Nature, 304, 156-158.
Backman, J. & Shackleton, N.J. (1983) Quantitative biochronology of Pliocene and early Pleistocene nannofossils
from the Atlantic, Indian and Pacific oceans. Marine Micropaleontology, 8, 141-170.
Bailey, G.N., Deith, M.R. & Shackleton, N.J. (1983) Oxygen isotope analysis and seasonality determinations: limits and potential of a new technique. American Antiquity, 48, 390-398.
Moore, T.C. Jr., Rabinowitz, P.D., Boersma, A., Borella, P.E., Chave, A.D., Duee, G., Futterer, D.K., Jiang, M.J.,
Kleinert, K., Lever, A., Manivit, H., O'Connell, S., Richardson, S.H. and Shackleton, N.J. (1983) The Walvis
Ridge transect, Deep Sea Drilling Project Leg 74: The geologic evolution of an oceanic plateau in the south
Atlantic Ocean. Geological Society of America Bulletin, 94, 907-925.
Shackleton, N.J. (1983) Isotopic composition of the ocean surface as a source for the ice in Antarctica. In: Robin,
G. de Q. (Ed.) The climatic record in the polar ice sheets. Part 3: Glaciological parameters, their measurement
and significance. Cambridge: Cambridge University Press, 43-47.
Shackleton, N.J. & Hall, M.A. (1983) Stable isotope record of Hole 504 sediments: high-resolution record of the
Pleistocene. In Cann, J.R., Langseth, M.G. et al., Init. Repts DSDP,69: Washington (U.S. Govt. Printing
Office), 69, 431-441.
Shackleton, N.J., Hall, M.A., Line, J. & Cang, S. (1983) Carbon isotope data in core V19-30 confirm reduced carbon dioxide concentration in the ice age atmosphere. Nature, 306, 319-322.
Shackleton, N.J., Imbrie, J. & Hall, M.A. (1983) Oxygen and carbon isotope record of East Pacific core V19-30:
implications for the formation of deep water in the late Pleistocene North Atlantic. Earth and Planetary
Science Letters, 65, 233-244.
Bath, A. & Shackleton, N.J. (1984) Oxygen and hydrogen isotope studies in squeezed pore waters, Deep Sea
Drilling Project Leg 74, Hole 525B: evidence for mid-Miocene Ocean isotopic change. In Moore, T.C. Jnr.,
Rabinowitz, P.D. et al., Init. Repts DSDP, 74:215

Washington (U.S. Govt. Printing Office), 74, 697-699.
Berggren, W.A., Nakagawa, H., Saito, T., Shackleton, N.J. & Shibata, K. (1984) Neogene Magnetostratigraphy andChronostratigraphy. In: Ikebe, N. & Tsuchi, R. (Eds.) Pacific Neogene Datum Planes: Contributions to
Biostratigraphy and Chronology. Tokyo: University of Tokyo Press, 83-84.
Duplessy, J.-C. & Shackleton, N.J. (1984) Carbon-13 in the World Ocean during the Last Interglaciation and thePenultimate Glacial Maximum. Reevaluation of the possible biosphere response to the Earth's climaticchanges. Progress in Biometeorology, 3, 48-54.
Duplessy, J.-C., Shackleton, N.J., Matthews, R.K., Prell, W., Ruddiman, W.F., Caralp, M. & Hendy, C.H. (1984)
13
C Record of benthic foraminifera in the last interglacial ocean: implications for the carbon cycle and theglobal deep water circulation. Quaternary Research, 21, 225-243.
Imbrie, J., Hays, J.D., Martinson, D.G., McIntyre, A., Mix, A.C., Morley, J.J., Pisias, N.G., Prell, W.L., andShackleton, N.J. (1984) The orbital theory of Pleistocene climate: support from a revised chronology of themarineδ18O record. In: Berger, A.L. et al., (Eds) Milankovitch and Climate, Part 1, D. Reidel Pub. Co., 269305.
Moore, T.C. Jr., Rabinowitz, P.D., Borella, P.E., Boersma, A., & Shackleton, N.J. (1984) Introduction and explanatory notes. In Moore, T.C. Jnr., Rabinowitz, P.D. et al., Init.Repts DSDP, 74: Washington (U.S. Govt. Printing
Office) 74, 3-39. Book contribution
Moore, T.C. Jr., Rabinowitz, P.D., Borella, P.E., Shackleton, N. J. & Boersma, A. (1984) History of the Walvis
Ridge. In Moore, T.C. Jnr., Rabinowitz, P.D. et al., Init. Repts DSDP, 74: Washington (U.S. Govt. Printing
Office), 74, 873-894.
Morley, J.J. & Shackleton, N.J. (1984) The effect of accumulation rate on the spectrum of geologic time series: evidence from two South Atlantic sediment cores. In: Berger, A.L. et al. (Eds.) Milankovitch and Climate. Part
1. Pub. D. Reidel, 467-480.
Pisias, N.G. & Shackleton, N.J. (1984) Modeling the global climate response to orbital forcing and atmospheric carbon dioxide changes. Nature, 310, 757-759.
Pisias, N.G., Martinson, D., Moore, T.C. Jr., Shackleton, N.J., Prell, W.L., Hays, J. & Boden, G. (1984) High resolution stratigraphic correlations of benthic oxygen isotopic records spanning the last 300,000 years. Mar.
Geol., 56, 119-136.
Shackleton, N.J. (1984) Oxygen isotope evidence for Cenozoic climatic change. In: Brenchley, P. (Ed.) Fossils andClimate. John Wiley & Sons Ltd., 27-34.
Shackleton, N.J. (1984) Pleistocene deep-sea sediment stratigraphy and its extension. In: Seibold, E. &Meulenkamp, J.D. (Eds.) Stratigraphy Quo Vadis? AAPG Studies in Geology No. 16. IUGS Special
Publication No. 14. Papers from a 1982 IUGS Commission on Stratigraphy Symposium, Bad Honnef, West
Germany, 15-19.
Shackleton, N.J. & Members of the Shipboard Scientific Party (1984) Accumulation rates in Leg 74 sediments. In
Moore, T.C. Jr., Rabinowitz, P.D. et al., Init. Repts DSDP, 74: Washington (U.S. Govt. Printing Office), 74,
621-643.
Shackleton, N.J. & Hall, M.A. (1984) Carbon isotope data from Leg 74 Sediments. In Moore, T.C. Jnr.,
Rabinowitz, P.D. et al., Init. Repts DSDP, 74: Washington (U.S. Govt. Printing Office), 74, 613-619.
Shackleton, N.J. & Hall, M.A. (1984) Oxygen and carbon isotope stratigraphy of Deep Sea Drilling Project Hole
552A: Plio-Pleistocene glacial history. In Roberts, D.G., Schnitker, D. et al. Init. Repts. DSDP, 81:
Washington: (U.S. Govt. Printing Office), 81, 599-609.
Shackleton, N.J., Backman, J., Zimmerman, H., Kent, D.V., Hall, M.A., Roberts, D.G., Schnitker, D., Baldauf, J.G.,
Desprairies, A., Homrighausen, R., Huddlestun, P., Keene, J.B., Kaltenback, A.J., Krumsiek, K.A.O., Morton,
A.C., Murray, J.W., & Westberg-Smith, J. (1984) Oxygen isotope calibration of the onset of ice-rafting and history of glaciation in the North Atlantic region. Nature, 307, 620-623.
Shackleton, N.J., Hall, M.A. & Boersma, A. (1984) Oxygen and carbon isotope data from Leg 74 foraminifers. In
Moore, T.C. Jnr., Rabinowitz, P.D. et al. Init. Repts. DSDP, 74: Washington: (U.S. Govt. Printing Office), 74,
599-612.
Wintle, A.G., Shackleton, N.J. & Lautridou, J.P. (1984) Thermoluminescence dating of periods of loess depositionand soil formation in Normandy. Nature, 310, 491-493.
Zimmerman, H.B., Shackleton, N.J., Backman, J., Kent, D.V., Baldauf, J.G., Kaltenback, A.J. & Morton, A.C.
(1984) History of Plio-Pleistocene climate in the northeastern Atlantic, Deep-Sea Drilling Project Hole 552A.

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In: Roberts, D.G., Schnitker, D., et al., Init. Repts. DSDP, 81: Washington (U.S. Govt. Printing Office), 81, 861876.
Duplessy, J.-C. & Shackleton, N.J. (1985) Response of global deep-water circulation to the Earth's climatic change
135,000-107,000 years ago. Nature, 316, 500-507.
Jenkins, D.G., Bowen, D.Q., Adams C.G., Shackleton N.J. & Brassell, S.C. (1985) The Neogene: Part 1. In:
Snelling, N.J. (Ed.) The Chronology of the Geological Record. Geological Society Memoir, 10, 199-210.
Pisias, N.G., Shackleton, N.J. & Hall, M.A. (1985) Stable Isotope and Calcium Carbonate Records from HydraulicPiston Cored Hole 574A: High resolution records from the Middle Miocene. In Mayer, L., Theyer, F. et al.
(Eds.), Init. Repts. DSDP, 85: Washington (U.S. Govt. Printing Office), 85, 735-748.
Shackleton, N.J. (1985) Oceanic carbon isotope constraints on oxygen and carbon dioxide in the Cenozoic atmosphere. The carbon cycle and atmospheric CO2: natural variations Archean to present. Geophysical
Monograph, 32, 412-417.
Shackleton, N.J., Corfield, R.M. & Hall, M.A. (1985) Stable isotope data and the ontogeny of Paleocene planktonic
foraminifera. Journal of Foraminiferal Research, 15, 321-336.
Shackleton, N.J., Hall, M.A. & Bleil, U. (1985) Carbon-isotope stratigraphy, Site 577. In Heath, G.R., Burckle,
L.H. et al. (Eds.), Init. Repts DSDP, 86: Washington (U.S. Govt. Printing Office), 86, 503-511.
Shackleton, N.J. & Pisias, N.G. (1985) Atmospheric carbon dioxide, orbital forcing and climate. In: E.T. Sundquist& W.S. Broecker (Eds.) The Carbon Cycle and Atmospheric CO2: Natural Variations, Archaean to Present.
Geophysical Monograph Series, 32, 303-317.
Wright, A.A., Bleil, U., Monechi, S., Michel, H.V. Shackleton, N.J., Simoneit, B.R.T. & Zachos, J.-C. (1985)
Summary of Cretaceous/Tertiary boundary studies, Deep Sea Drilling Project Site 577, Shatsky Rise. In Heath,
G.R., Burckle, L.H. et al. (Eds.), Init.Repts DSDP, 86: Washington: (U.S. Govt. Printing Office), 86, 799-804.
Chappell, J. & Shackleton, N.J. (1986) Oxygen isotopes and sea level. Nature, 324, 137-140.
Deith, M.R. & Shackleton, N.J. (1986) Seasonal exploitation of marine molluscs: oxygen isotope analysis of shellfrom La Riera Cave. In: Straus, L.G. & Clark, G.A. (Eds.) La Riera cave: Stone Age hunter-gatherer adaptations in northern Spain. Arizona State University Anthropological Research Papers, 36, 299-313.
Prell, W.L., Imbrie, J., Martinson, D., Morley, J., Pisias, N., Shackleton, N., & Streeter, H. (1986) Graphic correlation of oxygen isotope stratigraphy application to the late Quaternary. Paleoceanography, 1, 137-162.
Ruddiman, W.F., Shackleton, N.J., & McIntyre, A. (1986) North Atlantic sea-surface temperatures for the last 1.1
million years. In: Summerhayes, C.P. and Shackleton, N.J., (Eds.), North Atlantic Palaeoceanography,
Geol.Soc. Sp. Pub., 21, 155-173.
Shackleton, N.J. (1986) The Plio-Pleistocene oceans: stable isotope history. In: Hsü, K.J. (Ed.) Mesozoic andCenozoic Oceans. American Geophysical Union, Geodynamics Series, 15, 141-153.
Shackleton, N.J. (1986) Preface to 'Boundaries and Events in the Palaeogene'. Palaeogeography,
Palaeoclimatology, Palaeoecology, 57, 1-2.
Shackleton, N.J. (1986) Temperature history of the Earth's surface in relation to heat flow. In: Buntebarth G. andStegena, L., (Eds.) Lecture Notes in Earth Sciences. Paleogeothermics Springer-Verlag Berlin Heidelberg, 5,41-43, 205-228.
Shackleton, N.J. (1986) Paleogene stable isotope events. Palaeogeography, Palaeo-climatology,
Palaeoecology, 57, 91-102.
Summerhayes, C.P. & Shackleton, N.J. (Eds.) (1986) North Atlantic Palaeoceanography. Geological Society
Special Publication, 21.
Boersma, A., Premoli Silva, I. & Shackleton, N.J. (1987) Atlantic Eocene planktonic foraminiferal paleohydrographic indicators and stable isotope paleoceanography. Paleoceanography, 2, 287-331.
Martinson, D.G., Pisias, N.G., Hays, J.D., Imbrie, J., Moore, T.C. Jr., and Shackleton, N.J. (1987) Age dating andthe orbital theory of the ice ages: development of a high-resolution 0 to 300,000-year chronostratigraphy.
Quaternary Res., 27, 1-30.
Shackleton, N.J. (1987) The carbon isotope history of the Cenozoic: history of organic carbon burial and of oxygen in the ocean and atmosphere. In: Brooks J. & Fleet, A.J. (Eds.), Marine Petroleum Source Rocks.
Geological Society Special Publication. Oxford: Black-well, 26, 423-433.
Shackleton, N.J. (1987) Oxygen isotopes, ice volume and sea level. Quaternary Science Reviews, 6, 183-190.
Corfield, R.M. & Shackleton, N.J. (1988) Comment and Reply on "Danian faunal succession: Planktonic
foraminiferal response to a changing marine environment". Geology, 16, 378-380.

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Corfield, R. & Shackleton, N.J. (1988) Productivity change as a control on planktonic foraminiferal evolution after
the Cretaceous/Tertiary boundary. Historical Biology, 1, 323-343.
Curry, W. B., Duplessy, J.-C., Labeyrie, L. D. & Shackleton, N. J. (1988) Changes in the distribution ofδ13C ofdeep water ΣCO2 between the last glaciation and the Holocene. Paleoceanography, 3, 317-341.
Duplessy, J.-C., Shackleton, N. J., Fairbanks, R. G., Labeyrie, L. D., Oppo, D. & Kallel, N. (1988) Deepwater
source variations during the last climatic cycle and their impact on the global deepwater circulation.
Paleoceanography, 3, 343-360.
Shackleton, N.J., Duplessy, J.-C, Arnold, M., Maurice, P., Hall, M.A. & Cartlidge, J. (1988) Radiocarbon age oflast glacial Pacific deep water. Nature, 335, 708-711.
Shackleton, N.J., Imbrie, J. & Pisias, N.G. (1988) The evolution of oceanic oxygen-isotope variability in the North
Atlantic over the past three million years. Phil. Trans. Roy. Soc. Lond., B 318, 679-688. Book contribution
Shackleton, N.J., West, R.G. and Bowen, D.Q. (Eds.) (1988) The Past Three Million Years: Evolution of Climatic
Variability in the North Atlantic Region. Phil. Trans. R. Soc. Lond., B 318, 409-690.
Cang, S., Shackleton, N.J., Yunshan, Q. and Jun, Y. (1988) The discovery and significance of Globigerinoides
ruber (pink-pigmented) in Okinawa trough. Marine Geology & Quaternary Geology, 8, 24-30.
Hovan, S.A., Rea, D.K., Pisias, N.G. & Shackleton, N.J. (1989) A direct link between the China loess and marine
δ18O records: aeolian flux to the north Pacific. Nature, 340, 296-298.
Shackleton, N.J. (1989) Rosetta stone for Quaternary ice ages. Current Contents, 29, 15.
Shackleton, N.J. (1989) Deep trouble for climate change. Nature, 342, 616-617.
Shackleton, N.J. (1989) The Plio-Pleistocene ocean: Stable isotope history. In: Rose, J. & Schluchter, C. (Eds.),
Quaternary type sections: Imagination or Reality?, 11-24.
Chepstow-Lusty, A., Backman, J. & Shackleton, N.J. (1989) Comparison of upper Pliocene Discoaster abundance
variations from North Atlantic Sites 552, 607, 658, 659 and 662: further evidence for marine plankton responding to orbital forcing. In Ruddiman, W., Sarnthein, M. et al., Proc. ODP, Sci. Results, 108: College Station,
TX (Ocean Drilling Program), 108, 121-141.
Shackleton, N.J. & Hall, M.A. (1989) Stable isotope history of the Pleistocene at ODP Site 677. In Becker, K.,
Sakai, H. et al., Proc. ODP, Sci. Results, 111: College Station, TX (Ocean Drilling Program), 111, 295-316.
Andrews, J.E., Funnell, B.M., Jickells, T.D., Shackleton, N.J., Swallow, J.E., Williams, A.C. & Young, K.A.
(1990) Preliminary assessment of cyclic variations in foraminifers, barite and cadmium/calcium ratios in early
Pleistocene sediments from Hole 709C (equatorial Indian Ocean). In Duncan , R.A., Backman, J., Peterson,
L.C. et al., Proc. ODP, Sci. Results, 115: College Station, TX (Ocean Drilling Program), 115, 611-619. Book
contribution
Cang, S. & Shackleton, N.J. (1990) New technique for study on isotopic fractionation between sea water andforaminiferal growing processes. Chin. J. Oceanol. Limnol., 8, 299-305.
Grün, R, Shackleton, N.J. & Deacon, H. (1990) ESR dating of tooth enamel from Klasies River Mouth Cave, South
Africa. Current Anthropology, 31,427-432.
Labeyrie, L.D., Kallel, N., Arnold, M., Juillet-Leclerc, A., Maitre, F., Duplessy, J.-C. & Shackleton, N.J. (1990)
Variabilité des eaux intermédiaires et profondes dans l'océan Pacifique Nord-Ouest pendant la derniére
déglaciation. Oceanologica Acta, 10, 1-11.
Oppo, D.W., Fairbanks, R.G., Gordon, A.L. and Shackleton, N.J. (1990) Late Pleistocene Southern Ocean δ13C
variability: North Atlantic Deep Water modulation of atmospheric CO2. Paleoceanography, 5,1, 43-54.
Raymo, M.E., Ruddiman, W.F., Shackleton, N.J. & Oppo, D.W. (1990) Evolution of Atlantic-Pacific δ13C gradients over the last 2.5 m.y. Earth and Planetary Science Letters, 97,353-368.
Shackleton, N.J. (1990) Estimating atmospheric CO2. Nature, 347, 427-428.
Shackleton, N.J. (1990) Carbon isotope stratigraphy of bulk sediments, ODP Site 689 and 690, Maud Rise (datareport). In Barker, P.F, Kennett, J.P. et al., Proc.ODP, Sci. Results, 113: College Station, TX (Ocean Drilling
Program), 113, 985-989.
Shackleton, N.J., Berger, A. & Peltier, W.R. (1990) An alternative astronomical calibration of the Lower
Pleistocene timescale based on ODP Site 677. Transactions of The Royal Society of Edinburgh: Earth
Sciences, 81, 251-261.
Shackleton, N.J. & Hall, M.A. (1990) Pliocene Oxygen Isotope Stratigraphy of Hole 709C. In: Duncan, R.A.,
Backman, J., Peterson, L.C. et al., Proc. ODP, Sci. Results, 115: College Station, TX (Ocean Drilling
Program), 115, 529-538.

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Shackleton, N.J. & Imbrie, J. (1990) The δ18O spectrum of oceanic deep water over a five-decade band. Climate
Change, 16, 217-230.
Shackleton, N.J., van Andel, Tj.H., Boyle, E.A., Jansen, E., Labeyrie, L., Leinen, M., McKenzie, J., Mayer, L. &Sundquist, E. (1990) Contributions from the oceanic record to the study of global change on three time scales.
Palaeogeography, Palaeoclimatology, Palaeoecology, (Global and Planetary Change Section), 82, 5-37.
Stott, L.D., Kennett, J.P., Shackleton, N.J. & Corfield, R.M. (1990) The evolution of Antarctic surface waters during the Paleogene: inferences from the stable isotopic composition of planktonic foraminifera, ODP Leg 113.
In Barker, P.F. , Kennett, J.P. et al. Proc. ODP, Sci. Results, 113: College Station, TX (Ocean Drilling
Program), 113, 849-863.
Chepstow-Lusty, A., Backman, J. & Shackleton, N.J. (1991) Palaeoclimate control of Upper Pliocene Discoasterassemblages in the North Atlantic. Jour. Micropalaeontology, 9, 133-143.
Duplessy, J.-C., Bard., E., Arnold, M., Shackleton, N.J., Duprat, J. & Labeyrie, L. (1991) How fast did the oceanatmosphere system run during the last deglaciation? Earth and Planetary Science Letters, 103, 27-40.
Morley, J.J., Heusser, L.E., & Shackleton, N.J. (1991) Late Pleistocene/Holocene radiolarian and pollen records
from sediments in the Sea of Okhotsk. Paleoceanography, 6, 121-131.
Nansen Arctic Drilling Program NAD Science Committee (1991) The Arctic Ocean record: Key to Global change(Initial Science Plan). Polarforschung, 61/1, 1-102.
Thomas, E., Shackleton, N.J. & Hall, M.A. (1991) Carbon isotope stratigraphy of Paleogene bulk sediments, Hole
762C (Exmouth Plateau, Eastern Indian Ocean). In: von Rad, U., Haq, B.U. et al. Proc.ODP, Sci. Results, 122:
College Station, TX (Ocean Drilling Program), 1031-1035.
Vincent, E., Shackleton, N.J. & Hall, M.A. (1991) Miocene oxygen and carbon isotope stratigraphy of planktonic
foraminifers at Sites 709 and 758, tropical Indian Ocean. In Weissel, J., Peirce, J., Taylor, E., Alt, J., et al., Proc.
ODP, Sci. Results, 121: College Station, TX (Ocean Drilling Program), 121, 241-252. Book contribution
Chepstow-Lusty, A., Shackleton, N.J. & Backman, J. (1992) Upper Pliocene Discoaster abundance variations fromthe Atlantic, Pacific and Indian Oceans: the significance of productivity pressure at low latitudes. Memorie di
Scienze Geologiche, 44, 357-373.
Dia, A.N., Cohen, A.S., O'Nions, R.K. & Shackleton, N.J. (1992) Seawater Sr-isotope variation over the last 300
ka and global climate cycles. Nature, 356, 786-788.
Hagelberg, T., Shackleton, N.J., Pisias, N., & Shipboard Party (1992) Development of composite depth sections for
Sites 844 through 854. In Mayer, L., Pisias, N., Janecek, T., et al (Eds.) Proc. ODP, Init. Repts. 138: College
Station, TX (Ocean Drilling Program), 138, 79-85. Book contribution
Imbrie, J., Boyle, E.A., Clemens, S.C., Duffy, A., Howard, W.R., Kukla, G., Kutzbach, J., Martinson, D.G.,
McIntyre, A., Mix, A.C., Molfino, B., Morley, J.J.,Peterson, L.C., Pisias, N.G., Prell, W.L., Raymo, M.E.,
Shackleton, N.J. & Toggweiler, J.R. (1992) On the structure and origin of major glaciation cycles. 1. Linear
responses to Milankovitch forcing. Paleoceanography, 7, 701-738.
Labeyrie, L.D., Duplessy, J.-C., Duprat, J., Juillet-Leclerc, A., Moyes, J., Michel, E., Kallel, N. & Shackleton, N.J.
(1992) Changes in the vertical structure of the North Atlantic Ocean between glacial and modern times.
Quaternary Science Review, 11, 401-413.
Le, J. & Shackleton, N.J. (1992) Carbonate dissolution fluctuations in the western equatorial Pacific during the Late
Quaternary. Palaeoceanography, 7, 21-42.
Mayer, L., Pisias, N., Janecek, T. et al (including Shackleton, N.J.) (1992) Proc. ODP, Init. Repts., 138: College
Station, TX (Ocean Drilling Program), 138. Book contribution
Mayer, L., Pisias, N. & Shipboard Party (including Shackleton, N.J.) (1992) High-resolution studies of the Eastern
Equatorial Pacific. EOS, 73, 257-262.
Meynadier, L., Valet, J.-P., Weeks, R., Shackleton, N.J. & Lee Hagee, V., (1992) Relative geomagnetic intensityof the field during the last 140 KA. Earth Planet. Sci. Lett., 114, 39-57.
Shackleton, N.J., Le, J., Mix, A. & Hall, M.A. (1992) Carbon isotope records from Pacific surface waters andatmospheric carbon dioxide. Quat. Sci. Rev., 11, 387-400.
Shackleton, N.J. and Shipboard Party (1992) Sedimentation rates: towards a GRAPE density stratigraphy for Leg
138 carbonate sections. In Mayer, L., Pisias, N., Janecek, T., et al (Eds.) Proc. ODP, Init. Repts., 138: College
Station, TX (Ocean Drilling Program), 138, 87-91.
Bard, E., Stuiver, M. & Shackleton, N.J. (1993) How accurate are our chronologies of the past? In: J.A. Eddy &H. Oeschger (Eds.) Global Changes in the Perspective of the Past: Dahlem Workshop Reports, 12, 103-120.

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Gallée, H., Berger, A. & Shackleton, N.J. (1993) Simulation of the climate of the last 200 kyr with the LLN 2Dmodel. In: Peltier, W.R. (Ed.) Proceedings of the NATO ARW, Aussois, 112, 321-341
Hooghiemstra, H., Melice, J.L., Berger, A. & Shackleton, N.J. (1993) Frequency spectra and paleoclimatic variability of the high-resolution 30-1450 kyr Funza 1 pollen record (Eastern Cordillera, Colombia). Quat. Sci.
Rev., 12, 141-156.
Imbrie, J., Berger, A., Boyle, E.A., Clemens, S.C, Duffy, A., Howard, W.R., Kukla, G., Kutzbach, J., Martinson,
D.G., McIntyre, A., Mix, A.C., Molfino, B., Morley, J.J., Peterson, L.C., Pisias, N.G., Prell, W.L., Raymo,
M.E., Shackleton, N.J. & Toggweiler, J.R. (1993) On the structure and origin of major glaciation cycles 2. The
100,000-year cycle. Paleoceanography, 8, 699-735.
Imbrie, J., Berger, A. & Shackleton, N.J. (1993) Role of orbital forcing: a two-million year perspective. In J.A.
Eddy & H. Oeschger (Eds.) Global Changes in the Perspective of the Past: Dahlem Workshop Reports, 12,263-277.
Ivanova, E. & Shackleton, N.J. (1993) Paleoceanological conditions in the region of the East Pacific rise (21ES.L)
during the Middle-Late Quaternary. (In Russian) Oceanology, 33, 609-614.
Moore, T.C., Jr., Shackleton, N.J. & Pisias, N.G. (1993) Paleoceanography and the diachrony of radiolarian eventsin the eastern equatorial Pacific. Paleoceanography, 8, 567-586.
Pearson, P.N., Shackleton, N.J. & Hall, M.A. (1993) Stable isotope paleoecology of Middle Eocene planktonic
foraminifera and multi-species isotope stratigraphy, DSDP Site 523, South Atlantic. J. Foraminiferal Res., 23,
123-140.
Raffi, I., Backman, J., Rio, D. & Shackleton, N.J. (1993) Plio-Pleistocene nannofossil biostratigraphy and calibration to oxygen isotope stratigraphies from Deep Sea Drilling Project Site 607 and Ocean Drilling Program Site
677. Paleoceanography, 8, 387-408.
Shackleton, N.J. (1993) Last interglacial in Devils Hole. Nature, 362, 596.
Shackleton, N.J. (1993) The climate system in the recent geological past. Phil. Trans. R. Soc. Lond. B 341, 209213.
Shackleton, N.J., Hall, M.A., Pate, D., Meynadier, L., & Valet, J.-P. (1993) High resolution stable isotope stratigraphy from bulk sediment. Paleoceanography, 8, 141-148.
Bassinot, F.C., Labeyrie, L.D., Vincent, E., Quidelleur, X., Shackleton, N.J. & Lancelot, Y. (1994) The astronomical theory of climate and the age of the Brunhes/Matuyama magnetic reversal. Earth and Planetary Science
Letters, 126, 91-108.
Beveridge, N., Bertram, C., Elderfield, H. & Shackleton, N. (1994) δ13C-PO4 relationships in the glacial Atlantic.
Mineralogical Magazine, 58A, 83-84.
Beveridge, N.A.S. & Shackleton, N.J. (1994) Carbon isotopes in recent planktonic foraminifera: A record ofanthropogenic CO2 invasion of the surface ocean. Earth and Planetary Science Letters, 126, 259-273.
Chapman, M.R., Zhao, M., Eglinton, G. & Shackleton, N.J. (1994) Late Quaternary sea surface temperature records
from the North Atlantic: A comparison of molecular and faunal methods of paleotemperature estimation. EOS
Transactions, 75, 385-386.
Henderson, G.M., Martel, D.J., O'Nions, R.K. & Shackleton, N.J. (1994) Evolution of seawater 87Sr /86Sr over thelast 400ka: the absence of glacial/interglacial cycles. Earth and Planetary Science Letters, 128, 643-651
Heusser, L.E. & Shackleton, N.J. (1994) Tropical Climatic Variation on the Pacific Slopes of the Ecuadorian Andes
Based on a 25,000-Year Pollen Record from Deep-Sea Sediment core Tri 163-31 B. Quaternary Research, 42,
222-225.
Le, J. & Shackleton, N.J. (1994) Reconstructing paleoenvironment by transfer function: Model evaluation withsimulated data. Marine Micropaleontology, 24, 187-199.
Meynadier, L., Valet, J.P., Bassinot, F.C., Shackleton, N.J. & Guyodo, Y. (1994) Asymmetrical saw-tooth patternof the geomagnetic field intensity from equatorial sediments in the Pacific and Indian oceans. Earth andPlanetary Science Letters, 126, 109-127.
Shackleton, N.J. & Crowhurst, S. (1994) Details that make the difference. Oceanus, 36, 45-48.
Tauxe, L. & Shackleton, N.J. (1994) Relative paleointensity records from the Ontong-Java Plateau. Geophys.
Jour. Int., 117, 769-782.
Tiedemann, R., Sarnthein, M. & Shackleton, N.J. (1994) Astronomic timescale for the Pliocene Atlantic δ18O anddust flux records of ODP Site 659. Paleoceanography, 9, 619-638.
Bertram, C.J., Elderfield, H., Shackleton, N.J. & MacDonald, J.A. (1995) Cadmium/calcium and carbon isotope

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reconstructions of the glacial northeast Atlantic Ocean. Paleoceanography, 10, 563-578.
Berggren, W.A., Hilgen, F.J., Langereis, C.G., Kent, D.V., Obradovich, J.D., Raffi, I., Raymo, M.E. & Shackleton,
N.J. (1995) Late Neogene chronology: New perspectives in high-resolution stratigraphy. GSA Bulletin, 107,1272-1287.
Beveridge, N.A.S., Elderfield, H. & Shackleton, N.J. (1995) Deep thermohaline circulation in the low-latitude
Atlantic during the last glacial. Paleoceanography, 10, 643-660.
Curry, W.B., Shackleton, N.J., Richter, C., et al. (1995) Proc.ODP, Init. Repts., 154: College Station TX (Ocean
Drilling Program), 154. Book contribution
Leg 154 Scientific Party (Curry, Shackleton, Richter et al.) (1995) Ceara Rise Sediments Document: Ancient
Climate Change (ODP Leg 154) EOS, 76, 41-45
Hagelberg, T.K., Pisias, N.G., Mayer, L.A., Shackleton, N.J. & Mix, A.C. (1995) Spatial and temporal variabilityof Late Neogene equatorial Pacific carbonate: leg 138. In Pisias, N.G., Mayer, L.A., Janecek, T.R., PalmerJulson, A. & van Andel, T.H. (eds.). Proc. ODP, Sci. Results, 138: College Station, TX (Ocean Drilling
Program), 138, 321-336.
Hagelberg, T.K., Pisias, N.G., Shackleton, N.J., Mix, A.C. & Harris, S. (1995) Refinement of a high-resolution,
continuous sedimentary section for the study of equatorial Pacific paleoceanography: leg 138. In Pisias, N.G.,
Mayer, L.A., Janecek, T.R., Palmer-Julson, A. & van Andel, T.H. (eds.). Proc. ODP, Sci. Results, 138: College
Station, TX (Ocean Drilling Program), 138, 31-46.
Harris, S., Hagelberg, T., Mix, A., Pisias, N. & Shackleton, N.J. (1995) Sediment depths determined by comparisons of GRAPE and logging density data during ODP Leg 138. In Pisias, N.G., Mayer, L.A., and Janecek,
T.R., Palmer-Julson, A. and van Andel, T.H. (eds.). Proc. ODP, Sci. Results, 138: College Station, TX (Ocean
Drilling Program), 138, 47-57.
Kotilainen, A.T. & Shackleton, N.J. (1995) Rapid climate variability in the North Pacific Ocean during the past
95,000 years. Nature, 377, 323-326.
Le, J., Mix, A. & Shackleton, N.J. (1995) Late Quaternary Paleoceanography in the eastern equatorial Pacific
Ocean from planktonic foraminifers: a high-resolution record from ODP Site 846. In Pisias, N.G., Mayer,
L.A., Janecek, T.R., Palmer-Julson, A. & van Andel, T.H. (eds.). Proc. ODP, Sci. Results, 138: College Station,
TX (Ocean Drilling Program), 138, 675-694.
Manighetti, B., McCave, I.N., Maslin, M. & Shackleton, N.J. (1995) Chronology for climate change: Developing
age models for the Biogeochemical Ocean Flux Study cores. Paleoceanography, 10, 513-525
Maslin, M.A., Shackleton, N.J. & Pflaumann, U. (1995) Surface water temperature, salinity, and density changes
in the northeast Atlantic during the last 45,000 years: Heinrich events, deep water formation and climatic
rebounds. Paleoceanography, 10, 527-544
Meynadier, L., Valet, J.P. & Shackleton, N.J. (1995) Relative geomagnetic intensity during the last 4 million years
from the equatorial Pacific. In Pisias, N.G., Mayer, L.A., Janecek, T.R., Palmer-Julson, A. & van Andel, T.H.
(eds.). Proc. ODP, Sci. Results, 138: College Station, TX (Ocean Drilling Program), 138, 779-796.
Mix, A.C., Le, J. & Shackleton, N.J. (1995) Benthic foraminiferal stable isotope stratigraphy of Site 846: 0-1.8 MA.
In Pisias, N.G., Mayer, L.A., Janecek, T.R., Palmer-Julson, A. & van Andel, T.H. (eds.). Proc. ODP, Sci.
Results, 138: College Station, TX (Ocean Drilling Program), 138, 839-854.
Pearson, P.N. & Shackleton, N.J. (1995) Neogene multispecies planktonic foraminifer stable isotope record, Site
871, Limalok guyot. In Haggerty, J.A., Premoli Silva, I., Rack, F. & McNutt, M.K. (Eds.) Proc. ODP, Sci.
Results, 144: College Station, TX (Ocean Drilling Program), 144, 401-410.
Ravelo, A.C. & Shackleton, N.J. (1995) Evidence for surface water circulation changes at ODP Site 851 in the eastern tropical Pacific. In Pisias, N.G., Mayer, L.A., Janecek, T.R., Palmer-Julson, A. & van Andel, T.H. (eds.).
Proc. ODP, Sci. Results, 138: College Station, TX (Ocean Drilling Program), 138, 503-514.
Shackleton, N.J. (1995) New data on the evolution of Pliocene climatic variability. In: Vrba, E.S., Denton, G.H.,
Partridge, T.C., Burckle, L.H. (eds.), Paleoclimate and evolution with emphasis on human origins, Yale
University Press, 242-248.
Shackleton, N.J., An, Z., Dodonov, A.E., Gavin, J., Kukla, G.J., Ranov, V.A. & Zhou, L.P. (1995) Accumulation
rate of loess in Tadjikistan and China: Relationship with Global Ice Volume Cycles. Quaternary Proceedings,
4, 1-6.
Shackleton, N.J., Baldauf, J., Flores, J.-A., Iwai, M., Moore, T.C., Raffi, I. & Vincent, E. (1995) Biostratigraphic
summary for Leg 138. In Pisias, N.G., Mayer, L.A., Janecek, T.R., Palmer-Julson, A. & van Andel, T.H. (eds.).

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Proc. ODP, Sci. Results, 138: College Station, TX (Ocean Drilling Program), 138, 517-536. Book contribution
Shackleton, N.J., Crowhurst, S., Hagelberg, T., Pisias, N. & Schneider, D.A. (1995) A new Late Neogene timescale: application to ODP Leg 138 sites. In Pisias, N.G., Mayer, L.A., Janecek, T.R., Palmer-Julson, A. andvan Andel, T.H. (eds.). Proc. ODP, Sci. Results, 138: College Station, TX (Ocean Drilling Program), 138, 73101.
Shackleton, N.J., Hagelberg, T.K. & Crowhurst, S.J. 1995 Evaluating the success of astronomical tuning: Pitfalls
of using coherence as a criterion for assessing pre-Pleistocene timescales. Paleoceanography, 10, 693-697.
Shackleton, N.J. & Hall, M.A. (1995) Stable isotope records in bulk sediment, ODP Leg 138. In Pisias, N.G.,
Mayer, L.A., Janecek, T.R., Palmer-Julson, A. and van Andel, T.H. (eds.). Proc. ODP, Sci. Results, 138,
College Station, TX (Ocean Drilling Program), 138, 797-806.
Shackleton, N.J., Hall, M.A., & Pate, D. (1995) Pliocene stable isotope stratigraphy of ODP Site 846. In Pisias,
N.G., Mayer, L.A., Janecek, T.R., Palmer-Julson, A. and van Andel, T.H. (eds.). Proc. ODP, Sci. Results, 138:
College Station, TX (Ocean Drilling Program), 138, 337-356.
Shipboard Scientific Party (1995) Leg 154 Synthesis. In: Curry, W.B., Shackleton, N.J., Richter, C. et al. 1995,
Proc.ODP Init. Repts, 154: College Station, TX (Ocean Drilling Program), 154, 421-442.
Thomas, E., Booth, L., Maslin, M. & Shackleton, N.J. (1995) Northeastern Atlantic benthic foraminifera during thelast 45,000 years: Changes in productivity seen from the bottom up. Paleoceanography, 10, 545-562
Zhao, M., Beveridge, N.A.S., Shackleton, N.J., Sarnthein, M. & Eglinton, G. (1995) Molecular stratigraphy ofcores off northwest Africa: Sea surface temperature history over the last 80 ka. Paleoceanography, 10, 661675.
Zhou, L.P., Dodonov, A.E. & Shackleton, N.J. (1995) Thermoluminescence dating of the Orkutsay loess sectionin Tashkent Region, Uzbekistan, Central Asia. Quaternary Science Reviews, 14, 721-730.
Chapman, M.R., Shackleton, N.J., Zhao, M. & Eglinton, G. (1996) Faunal and alkenone reconstructions of subtropical North Atlantic surface hydrography and paleotemperature over the last 28 kyr. Paleoceanography, 11,343-357.
Kotilainen, A.T., Kotilainen, M.M., McCave, I.N. & Shackleton, N.J. (1996) Jääkausiajan ilmaston epävakaisuus
saa uusia todisteita. Geologi, 48, 51-57.
Maslin, M.A., Hall, M.A., Shackleton, N.J. & Thomas, E. (1996) Calculating surface water pCO2 fromforaminiferal organic δ13C. Geochimica et Cosmochimica Acta, 60, 5089-5100.
Pearson, P.N. & Shackleton, N.J. (1996) Stable isotopes and the enigma of planktonic foraminfer evolution, In:
Repetski, J.E. (ed.) Sixth North American Paleontological Convention, Abstracts. The Paleontological Society,
Special Publication, 8, 304.
Tauxe, L., Herbert, T., Shackleton, N.J., Kok, Y.S. (1996) Astronomical calibration of the Matuyama Brunhes
Boundary: Consequences for magnetic remanence acquisition in marine carbonates and the Asian loesssequences , Earth & Planetary Science Letters, 140, 133-146.
Thomas, E. & Shackleton, N.J. (1996) The Paleocene-Eocene benthic foraminiferal extinction and stable isotope
anomalies In: Knox, R. W. O'B., Corfield, R. M. & Dunnay, R.E. (eds.) Correlation of the early Paleogene inNorthwestern Europe, Geol. Soc. Spec. Publ., 101, 401-441.
Chapman, M.R. & Shackleton, N.J. (1997) Sub-Milankovitch fluctuations in North Atlantic latitudinal heat flux
during the last 150,000 years. Terra Nova, 9, 612.
King, T.A., Ellis, W.G., Jr., Murray, D.W., Shackleton, N.J. & Harris, S. (1997) Miocene evolution of carbonate
sedimentation at the Ceara Rise: A multivariate data/proxy approach. In Shackleton, N.J., Curry, W.B.,
Richter, C., et al. (Eds.), Proc. ODP, Sci. Results, 154: College Station, TX (Ocean Drilling Program), 154,349-365.
Maslin, M.A., Thomas, E., Shackleton, N.J., Hall, M.A. & Seidov, D. (1997) Glacial north east Atlantic surface
water pCO2: Productivity and deep-water formation. Marine Geology, 144, 177-190.
Pearson, P.N., Shackleton, N.J. & Hall, M.A. (1997) Stable isotopic evidence for the sympatric divergence ofGlobigerinoides trilobus and Orbulina universa (planktonic foraminifera). Journal of the Geological Society,London, 154, 295-302.
Pearson, P.N., Shackleton, N.J., Weedon, G.P. & Hall, M.A. (1997) Multispecies planktonic foraminifer stable isotope stratigraphy through Oligocene/Miocene boundary climatic cycles, site 926. In Shackleton, N.J., Curry,
W.B., Richter, C., et al. (Eds.), Proc. ODP, Sci. Results, 154: College Station, TX (Ocean Drilling Program),
154, 441-449.

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Shackleton, N.J. (1997) The deep-sea sediment record and the Pliocene-Pleistocene boundary. QuaternaryInternational, 40, 33-35.
Shackleton, N.J. & Crowhurst, S. (1997) Sediment fluxes based on an orbitally tuned time scale 5 Ma to 14 Ma,site 926 In Shackleton, N.J., Curry, W.B., Richter, C. & Bralower, T. (Eds.) Proc. ODP, Sci. Results, 154:
College Station, TX (Ocean Drilling Program, 154, 69-82.
Shackleton, N.J. & Hall, M.A. (1997) The late Miocene stable isotope record, site 926. In Shackleton, N.J., Curry,
W.B., Richter, C., et al. (Eds.), Proc. ODP, Sci. Results, 154: College Station, TX (Ocean Drilling Program),
154, 367-373.
Tzedakis, P.C., Andrieu, V., de Beaulieu, J.-L., Crowhurst, S., Follieri, M., Hooghiemstra, H., Magri, D., Reille,
M., Sadori, L., Shackleton, N.J. & Wijmstra, T.A. (1997) Comparison of terrestrial and marine records ofchanging climate of the last 500,000 years. Earth and Planetary Science Letters, 150, 171-176.
Weedon, G.P. & Shackleton, N.J. (1997) Inorganic geochemical composition of Oligocene to Miocene sediments
and productivity variations in the Western Equatorial Atlantic: Results from ODP sites 926 and 929. In
Shackleton, N.J., Curry, W.B., Richter, C., et al. (Eds.), Proc. ODP, Sci. Results, 154: College Station, TX(Ocean Drilling Program), 154, 507-526.
Weedon, G.P., Shackleton, N.J. & Pearson, P.N. (1997) The Oligocene time scale and cyclostratigraphy on the
Ceara Rise, Western Equatorial Atlantic. In Shackleton, N.J., Curry, W.B., Richter, C., et al. (Eds.), Proc. ODP,
Sci. Results, 154: College Station, TX (Ocean Drilling Program), 154, 101-114.
Chapman, M.R. & Shackleton, N.J. (1998) Millennial-scale fluctuations in North Atlantic heat flux during the last
150,000 years. Earth and Planetary Science Letters, 159, 57-70.
Chapman, M.R. & Shackleton, N.J. (1998) What level of resolution is attainable in a deep-sea core? Results of aspectrophotometer study? Paleoceanography, 13, 311-315.
Hall, I.R., McCave, I.N., Chapman, M.R., Shackleton, N.J. (1998) Coherent deep flow variation in the Iceland andAmerican basins during the last interglacial. Earth and Planetary Science Letters, 164, 15-21
Kroon, D., Norris, R.D., Klaus, A. et al. (1998) Proc. ODP Init. Repts, 171B: College Station TX (Ocean Drilling
Program). Book contribution
Kroon, D., Norris, R.D., Klaus, A. & the ODP LEG171B Shipboard Scientific Party (1998) Drilling Blake Nose:the search for evidence of extreme Palaeogene-Cretaceous climates and extraterrestrial events. Geology Today,
November December, 222-226.
Cacho, I., Grimalt, J.O., Pelejero, C., Canals, M., Sierro, F.J., Flores, J. A. & Shackleton, N.J. (1999) DansgaardOeschger and Heinrich event imprints in Alboran Sea paleotemperatures. Paleoceanography, 14, 698-705
Chapman, M.R. & Shackleton, N.J. (1999), Global ice-volume fluctuations, North Atlantic ice rafting events, anddeep-ocean circulation changes between 130 and 70 ka. Geology.27, 795-798
Dodonov, A.E., Shackleton, N., Zhou, L.P., Lomov, S.P. & Finaev, A.F.(1999) Quaternary Loess-Paleosol
Stratigraphy of Central Asia: Geochronology, Correlation, and Evolution of Paleoenvironments, Stratigraphy
and Geological Correlation, 7, 581-593
Gale, A.S., Young, J.R., Crowhurst, S.J., Shackleton, N.J. & Wray D.S. (1999) Orbital tuning of Cenomanian marly
chalk successions: towards a Milankovitch timescale for the Late Cretaceous. Proceedings of the Royal Societyof London A.357,1815-1829
Martin, E.E., Shackleton, N.J., Zachos, J.-C. and Flower, B.P. (1999) Orbitally-tuned Sr isotope chemostratigraphy for thelate middle to late Miocene. Paleoceanography, 14, 74-83.
〜
Sánchez Goni, M.F., Eynaud, F., Turon, J.-L. & Shackleton, N.J., (1999) High resolution palynological record off
the Iberian margin: direct land-sea correlation for the Last Interglacial complex. Earth and Planetary Science
Letters.171, 123-137
Shackleton, N.J., Crowhurst, S., Weedon, G. & Laskar, J. (1999) Astronomical Calibration of Oligocene-Miocene
Time. Proceedings of the Royal Society of London A., 357,1907-1929
Zhou, L.P. & Shackleton, N.J. (1999) Misleading positions of geomagnetic reversal boundaries in Eurasian loessand implications for correlation between continental and marine sedimentary sequences. Earth and Planetary
Science Letter, 168, 117-130.
Cacho, I., Grimalt, J.O., Sierro, F.J., Shackleton, N.J., Canals, M. (2000) Evidence for enhanced Mediterranean
thermohaline circulation during rapid climatic coolings. Earth and Planetary Science Letters, 183, 417-429
Chapman, M.R. & Shackleton, N.J. (2000) Evidence of 550-year and 1000-year cyclicities in North Atlantic circulation patterns during the Holocene. The Holocene, 10, 287-291

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Chapman, M.R., Shackleton, N.J. & Duplessy, J.-C. (2000) Sea surface temperature variability during the lastglacial-interglacial cycle: assessing the magnitude and pattern of climate change in the North Atlantic.
Palaeogeography, Palaeoclimatology, Palaeoecology, 157, 1-25
Coxall, H.K., Pearson, P.N., Shackleton, N.J., Hall, M.A. (2000) Hantkeninid depth adaptation: An evolving life
strategy in a changing ocean, Geology, 28, 87-90
Lear, C.H., Wilson, P.A., Shackleton, N.J., Elderfield, H. (2000) Palaeotemperature and ocean chemistry records
for the Palaeogene from Mg/Ca and Sr/Ca in benthic foraminiferal calcite. GFF, 122, 93
Pälike, H., Shackleton, N.J. (2000) Constraints on astronomical parameters from the geological record for the last
25 Myr Earthand Planetary Science Letters, 182, 1-14〜
Sánchez Goni, M.F., Turon, J.-L., Eynaud, F., Shackleton, N.J. & Cayre, O. (2000) Direct land/sea correlation of
the Eemian, and its comparison with the Holocene: a high-resolution palynological record off the Iberian margin. Geologie en Mijnbouw / Netherlands Journal of Geoscience, 79, 345-354
Sarnthein, M., Kennett, M.-S., Chappell, T., Crowley, T., Curry, W., Duplessy, C., Grootes, P., Hendy, I., Laj, C.,
Negendank, J., Schultz, M., Shackleton, N.J., Voelker, A., Zolitschka, B., and the other Trins workshop participants (2000) Exploring Late Pleistocene Climate Variations. EOS, 81, 628-631
Seidenkrantz, J.-P., Kouwenhoven, T.J., Jorissen, F.J., Shackleton, N.J. & van der Zwaan, B.J. (2000) Benthic
foraminifera as indicators of changing Mediterranean-Atlantic water exchange in the Late Miocene . Marine
Geology, 163, 387-407
Shackleton, N.J. (2000) The 100,000-Year Ice-Age Cycle Identified and Found to Lag Temperature, Carbon
Dioxide and Orbital Eccentricity. Science, 289, 1897-1902.
Shackleton, N.J., Hall, M.A., Raffi, I.,Tauxe, L.& Zachos, J. ( 2000) Astronomical calibration age for the
Oligocene-Miocene boundary. Geology, 28, 447-450
Shackleton, N.J., Hall, M.A. & Vincent, E. (2000) Phase relationships between Millennial Scale Events 64,000 to
24,000 Years Ago. Paleoceanography,15, 565-569
Thouveny, N., Moreno, E., Delanghe, D., Candon, L., Lancelot, Y. & Shackleton, N.J. (2000) Rock-magnetic
detection of distal ice rafted debris: clue for the identification of Heinrich layers on the Portuguese margin.
Earth and Planetary Science Letters, 180, 61-75
Zhou, L., Shackleton, N.J., Dodonov, A.E. (2000) Statigraphical interpretation of geomagnetic polarity boundaries
in Eurasian loess. Quaternary Sciences, 20, 196-202
Bianchi, G.G., Vautravers, M. & Shackleton, N.J. (2001) Deep flow variability under apparently stable North
Atlantic Deep Water production during the last interglacial of the sub-tropical NW Atlantic,
Paleoceanography, 16, 306-316
Cacho, I., Grimalt, J.O., Canals, M., Sbaffi, L., Shackleton, N.J., Schönfeld, J., Zahn, R. (2001) Variability of thewestern Mediterranean Sea surface temperature during the last 25,000 years and its connection with theNorthern Hemisphere climatic changes. Paleoceanography, 16, 40-52
Hall, I.R., McCave, I.N., Shackleton, N.J., Weedon, G.P. & Harris, S.E. (2001) The intensified deep Pacific inflow
and ventilation in Pleistocene glacial time. Nature, 412, 809-812
Klieven, H.F., Hall, I.R., McCave, I.N., Jansen, E., Shackleton, N.J. (2001) Reconstructing orbital-suborbital variability in deep water circulation in the North Atlantic across the mid-Pleistocene climate transition using thesortable silt current speed proxy. UK ODP Newsletter, 27, 34-35
Pälike, H., Shackleton, N.J., Röhl, U. (2001) Astronomical forcing in Late Eocene marine sediments. Earth andPlanetary Science Letters, 193, 589-602
Pearson, P.N., Ditchfield, P.W., Singano, J., Harcourt-Brown, K.G., Nicholas, C.J., Shackleton, N.J., & Hall, M.
(2001) Warm tropical sea-surface temperatures in the late Cretaceous and Eocene epochs. Nature, 413, 481487
Prokopenko, A.A., Karabanov, E.B., Williams, D.F., Kuzmin, M.I., Shackleton, N.J., Crowhurst, S.J., Peck, J.A.,
Gvozdkov, A.N. King, J.W. (2001) Biogenic Silica Record of the Lake Baikal Response to Climatic Forcing
during the Brunhes. Quaternary Research, 55, 123-132
Roucoux, K.H., Shackleton, N.J., de Abreu, L., Schönfeld, J. & Tzedakis, P.C. (2001) Combined Marine Proxy andPollen Analyses Reveal Rapid Iberian Vegetation Response to North Atlantic Millennial-Scale Climate
Oscillations. Quaternary Research, 56, 128-132
Sbaffi, L., Wezel, F.C., Kallel, N., Paterne, M., Cacho, I., Ziveri, P. & Shackleton, N.J. (2001) Response of thepelagic environment to palaeoclimatic changes in the central Mediterranean Sea during the Last Quaternary.

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Marine Geology, 178, 39-62
Shackleton, N.J. (2001) Climate Change Across the Hemispheres, Science, 291, 58-59
Tzedakis, P.C., Andrieu, V., de Beaulieu, J.L., Birks, H.J.B., Crowhurst, S., Follieri, M., Hooghiemstra. H., Magri,
D., Reille, M., Sadori, L. & Shackleton, N.J. & Wijmstra. T.A. (2001) Establishing a terrestrial chronologicalframework as a basis for biostratigraphical comparisons. Quaternary Science Reviews, 20, 1583-1592
Turco, E., Hilgen, F.J., Lourens, L.J., Shackleton, N.J., Zachariasse, W.J. (2001) Punctuated evolution of global climate cooling during the late Middle to early Late Miocene: High-resolution planktonic foraminferal and oxygen isotope records from the Mediterranean. Paleoceanography, 16, 405-423
Zachos, J.-C., Shackleton, N.J., Revenaugh, J.S., Pälike, H. & Flower, B.P.(2001) Climate Response to Orbital
Forcing Across the Oligocene-Miocene Boundary, Science, 292, 274-278
Zhou, L.P., Shackleton, N.J. (2001) Photon-stimulated luminescence of quartz from loess and effects of sensitivity change on palaeodose determination. Quaternary Science Reviews, 20, 853-857
Knutz, P.C., Hall, I.R., Zahn, R., Rasmussen, T.L., Kuijpers, A. Moros, M., Shackleton, N.J. (2002) Mutlidecal
ocean variability and NW European ice sheet surges during the last deglaciation. Geochemistry, Geophysics,
Geosystems.
Kukla, G.J., Bender, M.D., de Beaulieu, J.L., Bond, G., Broecker, W.S., Cleveringa, P.W., Gavin, J.E., Herbert,
T.D., Imbrie, J., Jouzel, J., Keigwin, L.D., Knudsen, K.L., McManus, J., Merkt, J., Muhs, D.R., Müller, H.,
Poore, R.Z., Porter, S.C., Seret, G., Shackleton, N.J., Turner, C., Tzedakis, P.C., Winograd, I.J. (2002) Last
Interglacial Climates. Quaternary Research, 58, 2-13
Marchal, O., Cacho, I., Stocker, T. F., Grimalt, J. O., Calvo, E., Martrat, B., Shackleton, N.J., Vautravers, M.,
Cortijo, E., van Kreveld, S., Andersson, C., Koç, N., Chapman, M.R., Sbaffi, L., Duplessy, J-C., Sarthein, M.,
Turon, J-L., Duprat, J., Jansen, E. (2002) Apparent long-term cooling of the sea surface in the Northeast
Atlantic and Mediterranean during the holocene. Quaternary Science Review, 21, 455-483
Martin, P.A., Lea, D.W., Rosenthal, Y., Shackleton, N.J., Sarnthein, M., Papenfusse, T. (2002) Quaternary deep sea
temperature histories derived from benthic foraminiferal Mg/Ca. Earth and Planetary Science Letters, 198,
193-209
Moreno, E., Thouveny, N., Delanghe, D., McCave, N., Shackleton, N.J.(2002) Climatic and oceanographic
changes in the Northeast Atlantic reflected by magnetic properties of sediments deposited on the Prtuguese
Margin during the last 340 ka. Earth and Planetary Science Letters, 202, 465-480
Pearson, P.N., Ditchfield, P., Shackleton, N.J.(2002) Tropical temperatures in greenhouse episodes (Zachos et al)- reply. Nature, 419, 898
Pérez,-Folgado, M., Sierro, F.J., Flores, J.A., Cacho, I., Grimalt, J.O., Zahn, R. Shackleton, N. J. (2003) Western
Mediterranean planktic foraminifera events and millennial climatic variability during the last 70 kiloyears.
Marine Micropaleontology,
v48, pp 49-70〜
Sánchez Goni, M.F., Cacho, I., Turon, J.L., Guiot, J., Sierro, F.J., Peypouquet, J.-P., Grimalt, J., Shackleton, N.J.
(2002) Synchroneity between marine and terrestrial responses to millennial scale climatic variability during thelast glacial period in the Mediterranean region.
Climate Dynamics, 19, 95-105〜
Shackleton, N.J., Chapman, M., Sánchez-Goni, M.F., Pailler, D. & Lancelot, Y. (2002) The Classic Marine Isotope
Substage 5e. Quaternary Research, 58, 14-16
de Abreu, L., Shackleton, N.J., Schönfeld, J., Hall, M.A. & Chapman, M. ( 2003) Millennial-scale oceanic climate
variability off the Western Iberian margin during the last two glacial periods. Marine Geology, 196, 1-20
Katz, M.E., Katz, D.R., Wright, L.D., Miller, G., Pak, D.K., Shackleton, N.J.& Thomas, E. (2003) Early Cenozoic
benthic foraminiferal isotopes: Species reliability and interspecies correction factors. Palaeoceanography, 18
Shackleton, N.J. (2003) Preliminary Report on the Molluscan Remains at Sitagroi. In: Prehistoric Sitagroi:
Excavations in Northeast Greece, 1968-1970 Vol 2 : The Final Report, Monumenta Archaeologia, 20, pp 361365〜
Shackleton, N.J., Sánchez-Goni, M.F., Pailler, D. & Lancelot, Y. ( 2003) Marine Isotope Substage 5e and theEemian Interglacial. Global and Planetary Change, 36, 151-155
Skinner, L.C., Shackleton, N.J. & Elderfield, H. (2003) Millennial-scale variability of deep-water temperature andδ18Odw indicating deep-water source variations in the Northeast Atlantic, 0-34 cal. ka.BP. Geochemistry
Geophysics Geosystems, vol 4, 1098
doi:10.1029/2003GC000585
Billups, K., Pälike, H., Channell, J., Zachos, J. & Shackleton, N.J. (2004) Astronomic calibration of the Late

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Oligocene through Early Miocene geomagnetic polarity time scale. Earth and Planetary Science Letters, 224,
33-44
Gibbs, S.J., Shackleton, N., Young, J. (2004) Orbitally forced climate signals in mid-Pliocene nannofossil assemblages. Marine Micropalaeonotology, 51, 39-56
Gibbs, S.J, Shackleton, N.J., Young, J.R. (2004) Identification of dissolution patterns in nannofossil assemblages:
a high-resolution comparison of synchronous records from Ceara Rise, ODP Leg 154. Paleoceanography, 19,
No1, PA1029
Lourens, L.J., Hilgen, F.J., Shackleton, N.J., Laskar, J., Wilson, D. (2004) The Neogene Period. In: A Geologic
Time Scale 2004, F. Gradstein, J. Ogg et al (eds), Cambridge University Press, 409-440
Moreno, A., Cacho, I., Canals, M., Grimalt, J.O., Sánchez-Goni, M.F., Shackleton, N.J., Sierro, F.J. ( 2005) Links
between marine and atmospheric processes oscillating on a milliennial time-scale. A multi-proxy study of thelast 50,000 yr from the Alborean Sea (Western Mediterranean Sea). Quaternary Science Review, 24, 16231636.
Pälike, H., Laskar, J. Shackleton, N.J. (2004) Geological constraints on the chaotic diffusion of the Solar System.
Geology, 32, 929-932
Pfuhl, H.A., Shackleton, N.J. (2004) Changes in coiling direction, habitat depth and abundance in two menardellid species. Marine Micropaleonotology, 50, 3-20
Pfuhl, H.A., Shackleton, N.J. (2004) Two proximal, high-resolution records of foraminiferal fragmentation andtheir implications for changes in dissolution. Deep-Sea Research, 51, 809-832
Shackleton, N.J., Fairbanks, R.G., Chiu, T.-C.., Parrenin, F. (2004) Absolute calibration of the Greenland timescale: implications for Antarctic time scales and for Δ14C. Quaternary Science Reviews. 23, 1513-1522
Skinner, L.C., Shackleton, N.J. (2004) Rapid transient changes in northeast Atlantic deep water ventilation-age
across Termination I. Paleoceanography, 19, PA2005, doi:10.129/2003PA000983
Tzedakis, P.C., Roucoux, K.H., de Abreu, L. Shackleton, N.J. (2004) The Duration of Forest Stages in Southern
Europe and Interglacial Climate Variability, Science, 306, 2231-2235
Vautravers, M.J., Shackleton, N.J., Lopez-Martinez, C., Grimalt, J.O. (2004) Gulf stream variability during Marine
isotope stage 3. Paleoceanography, 19, doi:10.1029/2003PA000966
de Abreu, L., Abrantes, F.F., Shackleton, N.J., Tzedakis, P.C., McManus, J.F., Oppo, D.W., Hall, M.A. (2005)
Ocean climate variability in the Eastern North Atlantic during interglacial MIS 11: A partial analogue to the
Holocene?, Paleoceanography, vol 20, doi:10.1029/2004PA001091
Gibbs, S.J., Young, J.R., Bralower, T.J. & Shackleton, N.J. (2005) Nannofossil evolutionary events in the mid
Pliocene: an assessment of the degree of synchrony in the extinctions of R. Pseudoumblicus and Sphenolithus.
Palaeogeography, Palaeoclimatology, Palaeoecology, 217, 155-172
Roucoux, K.H., de Abreu, L., Shackleton, N.J. & Tzedakis, P.C. (2005) The response of NW Iberian vegetation to
North Atlantic climate oscillations during the last 65kyr. Quaternary Science Reviews, 24, 1637-1653
Skinner, L.C., Shackleton, N.J.(2005 ) An Atlantic lead over Pacific deep-water change across Termination I;
implications for the application of the Marine Isotope Stage (MIS) stratigraphy. Quaternary Science Reviews,
24, 571-580
Ferretti, P., Shackleton, N.J., Hall, M.A. Rio, D. (2006) Early-Middle Pleistocene deep circulation in the western
subtropical Atlantic: Southern Hemisphere modulation of the North Atlantic Ocean. In: Early-Middle
Pleistocene Transitions: the land-ocean evidence. M.J. Head, P.L.Gibbard (eds) Geological Society of London,
Special Paper, 247, 131-145
Lea, D.W., Pak, D.K., Belanger, C.L., Spero, H.J., Hall, M.A. Shackleton, N.J. (2006) Paleoclimate history of
Galapagos surface waters over the last 135,000 yr. Quaternary Science Reviews, 25, 1152-1167
Vautravers, M.J., Shackleton, N.J. (2006) Centennial-scale hydrology off Portugal during marine isotope stage 3:
insights from Planktonic foraminiferal fauna variability. Paleoceanography, 21, doi 10.1029/2005PA001144

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Profile

Dr. Gordon Hisashi Sato
Director Emeritus, W. Alton Jones Cell Science Center, Inc.
Chairman of the Board, A&G Pharmaceutical, Inc.
President, Manzanar Project Corporation

Education and Academic and Professional Activities
1927
Born on December 17, in Los Angeles
1944
Graduated from Manzanar High School
1951
B.A., Biochemistry, University of Southern California
1953-1955 Teaching Assistant, Microbiology, California Institute of Technology
1955
Ph.D., Biophysics, California Institute of Technology
1958-1963 Assistant Professor, Graduate Department of Biochemistry, Brandeis University
1963-1968 Associate Professor, Graduate Department of Biochemistry, Brandeis University
1968-1969 Professor, Graduate Department of Biochemistry, Brandeis University
1969-1983 Professor, Biology Department, University of California, San Diego
1982
Rosentiel Award, Brandeis University
1983-1992 Director, W. Alton Jones Cell Science Center, Inc.
1984
Member, National Academy of Sciences
1987-present Distinguished Research Professor & Director of the Laboratory of Molecular
Biology, Clarkson University
1992-present Director Emeritus, W. Alton Jones Cell Science Center, Inc.
2002
The Rolex Awards for Enterprise
2002
Lifetime Achievement Award, Society for In Vitro Biology
2005
Distinguished Alumni Award of the California Institute of Technology

Dr. Sato has long dealt with the task of trying to cultivate food in a harsh environment, such asa desert, from his past experience of being relocated during World War II in a relocation campin the California desert for those of Japanese descent.
Dr. Sato was born on December 17, 1927 in Los Angeles as a child between a first-generation Japanese immigrant father and a second-generation mother. From his upbringing, hegrew up with traditional Japanese values such as social obligations and respect for humanfeelings. During World War II, he was relocated to Manzanar Relocation Camp in the
California desert with his family and this made a significant influence on his future way of life.
After the war, he studied biochemistry at University of Southern California and later
studied at California Institute of Technology under Max Delbruck who later received the Nobel
Prize in Physiology or Medicine. Max Delbruck not only taught him academically but also

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supported him economically, which changed Dr. Sato's life dramatically and he never forgot
the indebtedness he owed and nourished an idea that education was fundamental to bringing
up people, and he himself also provided opportunities for young people to get an education.
After doing research under Max Delbruck and earning a PhD in biophysics in 1955, hefurther carried out research at University of California at Berkley and University of Colorado
Medical School. In 1958, he became assistant professor of Graduate Department ofBiochemistry at Brandeis University in Massachusetts. He served as associate professor andprofessor at Brandeis till 1969, and moved to University of California San Diego (UCSD) andwas professor of biology there till 1983. There he succeeded in cell culturing in hormonallydefined medium devoid of serum and clarified that a specific hormone and a growth factor arenecessary for cells and made a significant contribution, scientifically mainly in mammaliancell culture.
While at UCSD in the early 1980s, he began to work on how to produce food in a severe
environment such as a desert, and started the research of growing algae in the desert withaquaculture utilizing the food chain in mind. In 1983, he moved from UCSD to the W. Alton
Jones Cell Science Center in Lake Placid, New York and began to work in earnest on the
Manzanar Project, which targeted to realize a healthy sustainable life even for those people
suffering hunger in a severe environment. After testing at production facilities built in the
Atacama Desert in Chile and in Fujian Province in China in the mid-1980s, a new location wassought and found Eritrea. Eritrea was under Ethiopian rule at that time and the people were
oppressed and suffered from starvation and Dr. Sato felt sympathy in its resemblance to thoseJapanese Americans during World War II. He began practicing aquaculture in the Northern
Eritrean coastline in 1986.
After Eritrea became independent, watching the camels eat mangrove leaves gave ahint and led to an idea that by utilizing mangroves as fodder, it will eventually be a more positive approach in enabling people to raise livestock and making them economically self-sustaining.
Mangroves only grew on 15% of Eritrean coastline. By disclosing that the seawater
lacked nitrogen, phosphorous and iron among the nutritional elements necessary for the mangrove to grow, he devised the basic technique to provide these elements slowly to the mangrove
and enabled the mangroves to be grown easily at low cost in areas where it was difficult togrow in the past. With this method, he succeeded in growing more than 800,000 mangrove
trees.
What Manzanar Project is aiming to do is to allow people living in a harsh environment
like a desert become self-sustaining by creating a sustainable economy. Dr. Sato's activities aredifferent from the previous aids from developed countries to Africa by not giving goods but
providing a mean of food production together with a mean for people to become self-sustaining, which indicates how future aids should be. His achievements which have proved a practical measure to enable economic self-sustainability in the poorest area of the world are significant and are demonstrating to the world the importance of a way of living which regularly
uses the technology of environmental conservation and humanity.

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EssayCreation of Mangrove Forests Where None Existed before
to Combat Hunger, Poverty and Global Warming
Dr. Gordon Hisashi Sato
An event of great importance to those interested in efforts to make the world a better place isthe contribution of a great deal of the fortune of Warren Buffet to the Bill and Melinda Gates
Foundation. Spending money effectively for humanitarian causes is a complicated and difficult process. In my experience, solving the technological problems is much simpler thanaddressing the problems that arise from cultural and political considerations. Warren Buffet
realized this and he is to be commended for acting rationally on this realization. The Gates
Foundation is an exceptionally well managed organization. This event has given me greatpause to reconsider what I and countless others are trying to do to correct the many ills of thisworld by relatively small individual efforts.
I had previously applied for funding from the Gates Foundation, and was told that thefoundation did not support efforts to combat hunger and poverty. A large foundation musthave policy guidelines and this makes them too inflexible to pursue unexpected opportunities
as they arise. In addition, the solutions to many of the world’s ills will come from unpredictable sources that will not fit in any conventional framework. I believe that I and many others of my ilk must continue to try to solve the many problems of this world and that collectively
we are an important part of the effort and will synergize with the large scale efforts of organizations like the Gates Foundation.
Let me now summarize what we have done and what we hope to do in the future. We
have shown that mangrove trees can be grown in desert inter tidal areas where they do not normally grow by providing them with phosphorus, nitrogen, and iron. This is because sea water
is deficient in these elements, and mangroves only grow where these elements are provided by
fresh water runoff from land. Though obvious, this fact is not generally understood by mangrove specialists. In addition, we have developed ways to deliver the fertilizer in the correctneeded amount so as to avoid waste and minimize the danger of fertilizer runoff. We havelearned to sun dry the seeds of Avicennia marina to produce a stable grain-like product that canserve as animal food several months after harvesting. We have learned that mangrove foliage
and seeds is an inadequate diet for sheep because they are able to produce lambs but cannot
produce the milk to feed them. By supplementing the mangrove material with a small amountof fish meal produced from fish wastes the sheep are able to produce lambs and milk. Thus
with simple experiments we are able to produce food and money for poor people where it did
not seem possible. We can convert barren mud flats into mangrove forests and use these toprovide the bulk of food for livestock. To date, we have grown about 800,000 mangrove trees
and potentially can grow many millions more in the country of Eritrea. This technology can229

reduce regional poverty in many parts of the world, and our present plan is to extend this work
to many impoverished regions of the world. In the next few months we will apply this technology in Haiti. Poverty and over population are two parts of the same problem. The solutionof one will be the solution of the other. In poor countries, people have many children to provide them support in their old age. This makes the prospect of a long term solution more difficult. In countries with a high standard of living such as Italy and Japan, population growth isnegative
We have developed a second way of producing food and wealth in poor coastal countries. The bottom of the food chain in the ocean is micro-organisms—mainly algae. They
grow very slowly by depending on sunlight for photosynthesis—about one doubling per day.
From our mangrove experience, we add nitrogen, phosphorus and iron to sea water and thenadd sugar. We get rapid growth of bacillus megatherium or the heterotrophic algae, tetraselmachui, and these in turn fed to filter feeders such as brine shrimp or shell fish. The brine shrimp
are then fed to fish. Thus we are able to convert a low cost commodity like sugar to a nutritious food with high economic value.
Global warming is on the minds of many people with apparent increased frequency andintensity of hurricanes. Some climatologist argue that there is insufficient evidence that this is
the result of increased output of green house gases by human activity. I respect their professional opinion, but I am sure if the CO2 content of the atmosphere continues to increase at thepresent rate it will eventually be the cause of catastrophe. We can only expect the output ofgreenhouse gases to increase as developing countries such as India, and China assume theirrightful places as nations with advanced industrialization and reasonable standards of living fortheir inhabitants. To fix the amount of CO2 produced from fossil fuels will require several hundred million hectares of new forests. I propose that we begin to convert the great deserts of theworld to mangrove forests with sea water irrigation. I believe our work has shown that this canbe technologically and economically feasible.
The work I have described is highly individualistic and unconventional. It is not thekind of work done by large organizations. It is too risky. Therefore I encourage people likemyself to continue to seek solutions to the ills of the world, and when these are well established, leave the large scale implementation to foundations such as the Gates Foundation.

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Lecture

Sea Water is Deficient in Nitrogen, Phosphorus and Iron
Dr. Gordon Hisashi Sato
The Manzanar Project, Ministry of Fisheries, State of Eritrea, Massawa, Eritrea
My scientific career was spent predominantly on laboratory research in cell biology. My goal
was to gain knowledge of whole animal physiology by studying the basic elements of the
body (the cell) in isolation under defined, controllable conditions which might be achievablein tissue culture. The trouble with this simple minded concept, in 1957, when I began work on
tissue culture, was that cells in culture did not display the differentiated properties of the tissue of origin. Apparently cells in culture were different from cells in the animal. It was generally believed that cells in culture underwent “dedifferentiation” to become a common tissue
culture type cell. In the only experiment to address this issue, we showed that when liver tissue is put into culture, the small amount of fibroblasts in the tissue selectively grow, and theliver parenchyma die1. The problem with lack of tissue specific properties in culture wasselection not “dedifferentiation.” The next step was to develop enrichment culture techniques
to favor tissue specific cells over fibroblasts2. This resulted in a number of tissue cultures
which retained differentiated properties, and the “dedifferention” hypothesis, virtually unnoticed, died a quiet death3 The next step was to devise defined, controllable conditions in culture. Traditionally, tissue culture media consisted of a nutrient solution of defined composition
supplemented with serum. I was led to believe that the serum could be replaced by hormones
because cell growth in the animal is stimulated by hormones4. Izumi Hayashi and I devised asystem of nutrient medium supplemented with a complex of hormones that was different foreach cell type5. This eliminated fibroblastic over growth in primary cultures, and made it possible to culture cell types never before successfully grown in culture. This method allows one
to discover hormone responses by different cell types discoverable in no other way, and I proposed that this catalogues the vulnerability of cancer cells and opens up a general approach tocancer therapy6. A case in point, we developed a monoclonal antibody to EGF receptor7. I was
led to try this approach from the knowledge of the existence of LATS, long acting thyroid stimulator, an antibody to the TSH receptor, which mimics the action of TSH. The antibody to the
EGF receptor has proven to be an effective anti cancer agent and is a harbinger of future anti
cancer agents8. I believe that my long experience with laboratory, experimental researchenabled me to approach applied, field research differently from established workers in thefield.
Let me now define the problem that has occupied me for the last twenty years. Hunger
and poverty is one of the problems that the human race must solve before it reaches a catastrophic, irreversible state. Eritrea is one of the poorest nations in the world with a per capita
gross domestic product of approximately 50 USD per year. Its conventional agriculture in its

231highlands is insufficient to feed the nation because of frequent and unpredictable droughts. In
periods of drought Eritrea would suffer widespread famine were it not for international foodaid. How could we produce food and a profitable, sustainable agriculture under such conditions? On its desert shores on the Red sea, I noticed patches of mangrove trees, and watchedcamels eating the foliage. Could this be a possible solution? But first we had to consider theconditions that limit the growth of mangroves. Sea water is deficient in nitrogen, phosphorus,
and iron, elements that are required by all living creatures including plants, animals and microorganisms. While this fact has been generally known, it has been ignored by those who areconcerned about the productivity of the sea and the inter tidal areas. I will try to show how
attention to this fact can help alleviate poverty and hunger by making the marine environment
more productive.Sea water contains all the elements in sufficient quantity that are essential forlife except for nitrogen, phosphorus and iron. So in the following discussion of the importanceof nitrogen, phosphorus, and iron, the term fertilizer will refer to these three elements. At thebottom of the food chain in the ocean are microscopic algae. They grow near the ocean surface where they are exposed to sunlight and capture the fertilizer. They sink to the bottom anddie from lack of light and the fertilizer is trapped. If upwelling currents bring up the fertilizer,
the sea is rich in fish. In the arctic and antarctic, water freezes and the saltier and heavier
unfrozen water sinks and stirs up the bottom. The polar regions are rich in fish life. Seas arerich in fish where rivers enter the sea because the fresh water is bringing fertilizer from land.
The Red sea has neither upwelling currents nor rivers. Consequently it is poor in fish life.
Eritrea has approximately 1,500 kilometers of desert sea coast along the Red Sea(counting islands). Mangroves grow in only about 15% of the coastal inter tidal zone, andwhere they grow they form a narrow fringe, usually no more than 100 meters wide. We
observed that mangroves typically occur in areas called “mersas” where the seasonal rains arechanneled to enter the sea each year. The conventional explanation is that fresh water per se isrequired9. This explanation is untenable because the amount of fresh water and the durationof flow are too short to affect salinity to any extent. Our explanation, which is a radical departure from conventional belief, is that the fresh water is bringing nitrogen, phosphorus, and ironfrom land, and the fringes are no more than 100 meters wide because the fresh water may not
be able to carry these minerals in sufficient quantity more than 100 meters from the high tideline. We predicted that the treeless, inter tidal areas of Eritrea, which occupy 85% of the coast,
could be successfully planted with mangroves if nitrogen, phosphorus, and iron were provided, and that the mangrove fringes could be widened if the trees were provided with theseelements.
Both of these predictions have proven true. Methods were developed to deliver fertilizer at a controlled rate that greatly reduces the possibility of runoff. Experiments were carried out to find ways of rendering mangrove foliage and seeds a complete food for livestock.
Materials and Methods
We use predominately the mangrove, Avicennia marina, and to a much lesser extent
Rhizophora mucronata. Both plants are indigenous to the area. Rhizophora are almost extinct
in Eritrea because of their value as construction timber. Our plantings will contribute to its

232preservation. Avicennia seeds are planted in their final site by placing them in a tin can cylinder constructed by removing the top and bottom of the tin can. The can is embedded in the soil
with a centimeter or so above the ground and is held in place with an iron rod. The top of the
can is covered with a wire mesh to prevent the seeds from being washed away by wave action.
Planting seeds in the final site saves considerably in time and effort by avoiding the necessityof transplantation. To prevent encircling wrasse and wave action from uprooting young
seedlings, we build concrete blocks with upwardly protruding iron rods. The dimensions of
the blocks are 1 meter long, about 25 centimeters high and about 5 centimeters wide with the
protruding iron rods about 60 centimeters above the blocks. A continuous wall of blocks isplaced sea ward of the area of planting. The iron rods prevent wrasse from entering the planting area, and the concrete blocks allow the buildup of low lying soil so that adequate drainage
can allow air to get to the roots. This allows the extension of the usable planting area.
Our method of providing a slow release fertilizer to trees growing in an area continuallyawash in sea water is to place 500 gms of a 3:1 mixture of urea and diammonium phosphatein a polyethylene bag, tie the bag so it is sealed shut, and puncture one surface three times witha 0.2 cm diameter nail. The bag is buried next to the tree with its upper surface and the nailhole punctures about 10.0 cm below the soil surface. This arrangement allows the fertilizer toexit the bag by slow diffusion - fast enough to nourish the tree but slow enough not to be
wasteful. By digging up bags after various times, we estimated that the bags deliver all theirfertilizer in about three years. From the density of planting, 5000 trees per hectare, we estimatethat the fertilizer is delivered at a rate of about one ton per hectare per year. This is approximately the desired rate. The desired rate is calculated as follows: a hectare of Avicennia drops
about 10 tons of litter per year which is about 19% protein, or two tons of protein. We assume
that the trees synthesize three tons of protein per hectare per year. To synthesize three tons ofprotein requires about one ton of fertilizer.
A barbed wire fence is erected around the trees and guards are employed to prevent
camels from destroying the trees.
To measure possible fertilizer runoff, water was collected a few meters offshore fromour plantings and from a natural mangrove forest about a half hour before the tide reached its
lowest level. The water was analysed for nitrogen and phosphorus content by the analyticallaboratory of the Ministry of Fisheries by the method of Parsons et al10.
Avicennia seeds are soaked in sea water for three days to remove the cover and facilitate drying. They are then placed in the sun to dry resulting in a grain-like material that isavidly eaten by animals up to a year after drying.
Results
Figure 1 shows a planting that is about 1 year old. No trees grew in this area before we planted
it. Before we realized the need for fertilizer, over a hundred trees were planted in this area andall died. After the need for fertilizer was understood, virtually all trees grew successfully with
our method of fertilization.
Figure 2 shows the same area about two years later. Growth is rapid.
Table 1 shows the measurement of nitrogen and phosphorus offshore from our planti-

233

ngs and offshore from a natural mangrove forest which was not fertilized by us compared to
the fertilizer content of water from the open sea. It can be seen that offshore from our plantings where three tons of fertilizer is applied per hectare no evidence of nitrogen or phosphorus
runoff is found. Offshore from a natural mangrove forest, nitrogen and phosphorus levels areappreciably higher than the open sea. This tends to support our assumption that natural mangrove forests are provided with fertilizer by the seasonal rains.
Figure 3 shows the concrete blocks with their protruding iron rods. They prevent wrasse
from entering the planting area and cause the build up of soil. Waves bring sand over theblocks and the sand is prevented by the blocks from returning seaward. By building up low
lying soil the usable planting area can be extended seaward.
Figure 4 shows our method of drying mangrove seeds to make a stable grain-like product that can serve as animal food several months after drying.
Figure 5 shows the drying of fish wastes to form fish meal that is an essential supplement to mangrove foliage and seeds for the feeding of livestock.
Figure 6 shows sheep eating mangrove foliage. They are also fed mangrove seeds andfish meal. They have been kept on such a diet for 8 months and produce babies and milk tofeed them. When the fish meal is omitted, they produce lambs but not the milk to feed them.
Figure 7 Camel lusting after mangrove trees.
Figure 8 A grove of trees in the village of Hargigo, our principal site of work. We haveplanted over 800,000 trees mainly in areas where trees had not grown before.
Figure 9 Typical housing in Hargigo reflective of the poverty in the region.
Figure 10 The water supply of the village which is shared with animals. One of ourmost urgent needs is a supply of healthy water.
Figure 11 Passengers from the Japanese peace boat visiting our work site in Hargigo
Discussion
Sea water is deficient in nitrogen, phosphorus, and iron . It follows that plants growing in theinter tidal area must have a source of these minerals. This is almost always furnished by fresh
water from land. In arid countries, areas where fresh water enters the inter tidal area are limited. It is in these areas where mangroves grow naturally. We have developed new ways of
substantially increasing the mangrove forests in tropical coastal deserts by making it possible
to grow mangroves in the tree less mud flats by artificially providing these elements. Such mud
flats make up the greater part of the inter tidal area of these coastal deserts. Even in tropicalcountries with plentiful rain, we can increase mangrove forests by widening the growth areaby fertilization and the use of concrete blocks. This can potentially reduce the damage due totsunamis, and hurricanes. We have also shown that mangroves can provide the bulk of the foodfor sheep with small and inexpensive supplementation of fish meal. This last finding renders
mangrove planting a technically feasible and commercially profitable business. We estimatethat a hectare of mangroves can produce a metric ton of meat per year. This compares favorably with pasture land in temperate climates. This should provide the economic incentive toplant mangroves as well as the disincentive to destroy them. Each of these findings is very simple but new and original. We believe that our approach has the potential to create a cost effec-

234

tive sea water agriculture and eliminate hunger and poverty in many regions of the world.
We believe that discoveries made in Africa can help solve problems in the developed
world, such as in Japan which produces only forty percent of its food. Algae in the ocean
divides about once a day. Simon Tecleab Gebrekiros and I discovered, in Eritrea, that we could
add nitrogen, phosphorus, iron, and sugar to sea water and get micro-organisms, bacteria oralgae, to divide every half hour. These micro-organisms were consumed by brine shrimp which
could then be fed to fish. By this method, we could make the coastal waters of any nation richin fish by essentially converting sugar to fish. Japan, for instance, could be made self sufficientfor fish. The coastal, inter tidal zones of Japan’s southern islands is nearly bereft of plants, andtheir fish catch is declining. Japanese control their fresh water so well that natural flows into
the sea is diminished. We can grow native plants in these inter tidal areas with fertilization andincrease fish life.
Mangroves seem to be limited by latitude. This fact is not well understood6. In northAfrica and southern Europe mangroves cannot grow because the tidal variation in the
Mediterranean and Aegan sea is too small to provide drainage and air to the roots. This raises
the possibility that mangroves could be grown inland, the Sahara desert for instance. Somecrop plants like millet and barley can grow with sea water irrigation, but the value of the cropis less than the cost of fertilizer and pumping water. Our trees have economic value, and wehave solved the problem of economic use of fertilizer. Can we pump sea water economicallywith for instance wind mill pumps. If so it is thinkable to convert the deserts of the world tomangrove forests. It is time to consider such far out solutions. Glacial ice is breaking off thepolar ice caps, the arctic tundra is melting, and typhoons and hurricanes are increasing in frequency and intensity. At present we add about four billion tons of CO2 to the atmosphere eachyear. As developing nations, such as India and China, assume their rightful positions as nations
with advanced industrialization and a high standard of living for their inhabitants, this will only
get worse. I believe converting the worlds deserts to forests is a necessary step to buy us time
before we can develop alternate forms of energy.
References
1. Sato G., L. Zaroff, and S.E. Mills 1960. Tissue Culture Populations and Their Relation to the Tissue of Origin.
Proc. Nat. Acad. of Sci. USA 46, 963-972
2. Buonassisi V., G. Sato, and A.I. Cohen. 1962. Hormone Producing Cultures of Adrenal and Pituitary Origin.
Proc. Nat. Acad, of Sci. USA 48. 1184-1190
3. Sato G.H., and Y. Yasumura. 1966. Retention of Differentiated Function in Dispersed Cell Culture. Transactionsof the New York Acad. of Sci, Ser 11 28:8 1063-1079
4. Sato, G. (1975) The Role of Serum in Cell Culture. In. Biochemical Action of Hormones. Vol. III (G. Litwak,ed.) pp. 391-396, Academic Press Inc., New York, San Francisco, London.
5. Hayashi I, and G. Sato 1976. Replacement of Serum with Hormones Permits the Growth of Cells in a DefinedMedium. Nature 259, 132-134
6. Sato G. (1980) Towards an endocrine physiology of human cancer. In. Hormones and Cancer ( S Iacobelli etal. eds.), Raven Press, N.Y. pp 281-285.
7. Sato J.D., T. Kawamoto, A.D.Le, J. Mendelsohn, J. Polikoff, and G.H. Sato (1983) Biological effects in vitro
or monoclonal antibodies to human EGF receptors. Mol. Biol. Med. 1:511-529
8. Masui H., T. Kawamoto, J.D. Sato, B. Wolf, J. Mendelsohn, and G. Sato. 1984. Growth Inhibition of Human
Tumor Cells in Nude Mice by anti-EGF Receptor Monoclonal Antibodies. Cancer Research 44, 1002-1007
9. Mark Spalding, Francois Blasco, and Colin Field. 1977 World Mangrove Atlas pp. 29. The International
Society for Mangrove Ecosystems, Okinawa, Japan

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10. Timothy R. Parsons, Yoshiaki Maita, and Carol M. Lalli. 1984. A Manual of Biological and Chemical Methods
for Seawater Analysis. Pergamon Press, New York236

Figure 1. Mangrove planting in area where mangroves had not grown before. About a year after planting.

Figure 2. Same scene as in previous slide, but three years after planting

237

Figure 3. Concrete blocks with protruding iron bars. In final position they build up soil on landward side.

Figure 4. Peeled Avicennia seeds drying in the sun

238

Figure 5. Fish wastes being sun dried after brief boiling.

Figure 6. Sheep eating mangrove foliage.

239

Figure 7. Camel lusting after mangrove trees.

Figure 8. Mangrove grove in village of Hargigo.

240

Figure 9. Typical housing in Hargigo

Figure 10. Source of village water.

241

Figure 11. Passengers from Japanese Peace Boat visiting the work site in Hargigo.

Table 1. Analysis of fertilizer content of seawater offshore from our plantings, offshore from a natural mangrove
forest, and from the open sea.
Nitrogen content

Inorganic phosphate

Area A in Hargigo with
3 tons of fertilizer per hectare

Not detectable.04 mg/liter

Area B in Hargigo with
3 tons of fertilizer per hectare

Not detectable.03 mg/liter

Natural mangrove forest
unfertilized.02 mg NH3/liter.01 mg NO3/liter.04 mg/liter

Water from open sea

not detectable.06 mg/liter

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Acknowledgments
Petros Solomon as Minister of fisheries had independently conceived of biosaline agriculture
as a way of building the economy of the country and gave enthusiastic support to the Manzanar
Project. We are grateful to his successor Ahmed Haj Ali for continuing the support. Financial
support was provided by the Ministry of Fisheries. A substantial grant was awarded to the
Manzanar Project by the Bruce and Giovanna Ames Foundation. Bruce Ames and Gordon
Sato were graduate students at the California Institute of Technology in the 1950s andGiovanna Ames grew up in Eritrea. A timely contribution from Mr. Edwin Joseph enabled the
Manzanar Project to continue when it was about to end for lack of funds. Gordon Sato
expresses gratitude to Mr. Shingo Nomura for providing funds early in the Manzanar program
which enabled him to provide material aid to the Eritreans during their struggle for independence. The Rolex Award for Enterprise of 2002 was awarded the Manzanar Project. We gratefully acknowledge its recognition and encouragement. Personal contributions were made andgratefully acknowledged from Dr. Dwight Robinson, Dr. Haile Debas, Dr. Ray Owen, Dr. T.T.
Puck, Dr. Robert Metzenberg, Dr. John Holland, Dr. Don Fawcett, Dr. Bruce Ames, Dr.
Giovanna Ames, Dr. Leona Wilson, Mr. Ed Welles, Mr. Carl Hodges, members of the
Manzanar high school class of 1944, members of JAACT and hundreds of private individuals.
Gordon Sato is grateful to the members of the Manzanar committee for their encouragement,
Kei Arima*, Thomas Maciag*, Stanely Cohen, Lawrence Grossman, Niels Jerne*, Rita Levi
Montalcini, Shingo Nomura, Martin Rodbell*, Jesse Roth, Jonas Salk*,Howard
Schneiderman*, Susumu Tonegawa, Lewis Thomas*, Gary Trudeau and James Watson.
*deceased

243

Follow-up Essay Contributed in June, 2013

Seawater Agriculture Can Solve
Many of the World's Problems
Dr. Gordon Hisashi SatoFirst we have to examine algae medium. All plants require all the elements in algae medium,from the tallest pine tree to the smallest seaweed to food crops such as corn and wheat. All
plants require all the elements found in algae medium and do not require any elements notfound in algae medium. There are exceptions to this generalization but they are very rare anddo not require our attention.
All food derives from plants. Lions and tigers eat grass but the grass must first be
eaten by deer and antelope.
Seawater contains all the elements in algae medium in sufficient quantities except forphosphorous, iron, and nitrogen. If these elements are added to seawater then any plant thatcan grow in seawater can be successfully grown in this fortified seawater; eg, one million
mangrove trees in Eritrea.
This fact presents an immediate solution to the problems of the Middle East. Unrest in
the Middle East is caused by poverty and unemployment. Even a country such as Saudi Arabia
with immense oil wealth has 30 to 40 percent unemployment.
The deserts of the Middle East could be fertilized with fortified seawater and crops
such as mangrove trees, spartina, and nitraria retusa could be grown for animal fodder.
Land based agriculture was first found to be feasible where fresh water naturally occurred.
This area was greatly expanded by digging trenches, and by using water pumps and animal
dung.
Some of the areas of the seas are very rich with the growth of seawater plants. Fertile
seabeds have developed where there is rain and as the rain moves over the land the streams offresh water dissolve needed minerals and deposit them in the ocean. No attempt was made toincrease the area of fertile seabeds. This is because the application of fertilizer was also foundto promote the growth of toxic algae such as red tide and microscopic algae which blocks the
sun from reaching useful plants, such as eelgrass, on the seabottom.
But toxic algae and useful seaplants both require the same nutrients. Therefore,
withholding fertilizer is not the solution to the problem because beneficial seaplants are also
discouraged.
We have developed a method of fertilizing useful plants to produce fertile seawater insuch a way that algae are discouraged and useful plants are supported. We make bricks of 1 lbof cement, 2 lb of gypsum, 1 lb of urea and 1 lb of phosphate. These bricks are placed on theocean bottom where some seaweed is growing and a small amount of iron is placed nearby.
The slowly dissolving bricks preferentially fertilize the ocean plants attached on the bottom
and the fertilizer which rises above the seabed are absorbed by the leaves and stems of theseaweed.
Algae typically has a 24 hour differentiation time. After division algae must accumulate
mineral nutrients and biosynthesize many components. Since algae are easily moved by water
currents and since the area of fertilizer is restricted near the ocean bottom the algae are not
likely to find themselves in a nutrient rich area and, therefore, massive growth of algae does
not occur.
We have observed that this method of fertilizing seawater brings about the growth of
eelgrass and brown, green and red seaweed and does not support the growth of algae.
This expansion of seaplants greatly increases fish and crabs.
The creation of wealth in poor countries with high unemployment and extreme poverty
can bring about the best solution for managing the expanding population of the world. The
most humane way to manage population growth is to increase the wealth of all its citizens.
Each year the world produces more than 32 billion tons of CO2 by burning fossil fuels.
It is very unrealistic to think that China and India will stop building coal fired power plants.
Land based plants can only fix about 60 percent of this CO2 and all arable land is alreadyutilized.
Seawater plants in coastal seabeds can absorb all the CO2 produced by fossil fuels
which then helps us to focus on the critical problem; methane gas produced by the melting
tundra.
In addition, ponds of seawater fertilized by phosphorous, iron, and nitrogen can produce
immense quantities of algae which can be pumped into depleted oil fields and replenish the oil
supply.