Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific
Identifieur interne : 000583 ( Istex/Corpus ); précédent : 000582; suivant : 000584Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific
Auteurs : A. M. Korotky ; N. G. Razjigaeva ; T. A. Grebennikova ; L. A. Ganzey ; L. M. Mokhova ; V. B. Bazarova ; L. D. Sulerzhitsky ; K. A. LutaenkoSource :
- The Holocene [ 0959-6836 ] ; 2000-04.
Abstract
Natural middle-and late-Holocene environmental development of Kunashiri Island reflects global climatic changes and the migration of warm and cold currents. Dry and cool climate changed to warm and moist about 7000–6500 BP, later than on Hokkaido Island. At this time Kuroshio Current system became more active. On Kunashir Island birch assemblages were replaced by cool-temperate broadleaf forests in the south and mixed coniferous/broadleaf forests in the north. The highest sea-level position reached 2.5–3 m above PSL about 6500–6300 BP. Cooling about 4700–4500 BP island vegetation weakly changed that connected with warm current influence. Major regression at this period led to formation of extensive coastal dunefields. The warming at the beginning of the late Holocene was almost similar to the Holocene Optimum. Two minor transgressions are recorded about 4010–3400 and 2950–2620 BP. Active entrance of detrital material to the coastal zone resulted in growth of accumulative landforms. Vegetation changes and climatic deterioration took place in the second half of the late Holocene. Coniferous and mixed coniferous/broadleaf forests shifted southward and occupied a large part of the island. During cooling at 1700–1300 BP the isthmus area increased, coastal wetlands with lakes and coastal dunes were formed, and grassland and swamp landscapes developed. Late-Holocene warming was not intensive. Active aeolian accumulation took place during the ‘Little Ice Age’ cooling and regression.
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DOI: 10.1191/095968300667552216
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A. Ganzey</name></author><author wicri:is="90%"><name sortKey="Mokhova, L M" sort="Mokhova, L M" uniqKey="Mokhova L" first="L. M." last="Mokhova">L. M. Mokhova</name></author><author wicri:is="90%"><name sortKey="Bazarova, V B" sort="Bazarova, V B" uniqKey="Bazarova V" first="V. B." last="Bazarova">V. B. Bazarova</name><affiliation><mods:affiliation>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Sulerzhitsky, L D" sort="Sulerzhitsky, L D" uniqKey="Sulerzhitsky L" first="L. D." last="Sulerzhitsky">L. D. Sulerzhitsky</name><affiliation><mods:affiliation>Geological Institute of Russian Academy of Sciences, Moscow, Russia</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Lutaenko, K A" sort="Lutaenko, K A" uniqKey="Lutaenko K" first="K. A." last="Lutaenko">K. A. 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M." last="Korotky">A. M. Korotky</name></author><author wicri:is="90%"><name sortKey="Razjigaeva, N G" sort="Razjigaeva, N G" uniqKey="Razjigaeva N" first="N. G." last="Razjigaeva">N. G. Razjigaeva</name><affiliation><mods:affiliation>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Grebennikova, T A" sort="Grebennikova, T A" uniqKey="Grebennikova T" first="T. A." last="Grebennikova">T. A. Grebennikova</name></author><author wicri:is="90%"><name sortKey="Ganzey, L A" sort="Ganzey, L A" uniqKey="Ganzey L" first="L. A." last="Ganzey">L. A. Ganzey</name></author><author wicri:is="90%"><name sortKey="Mokhova, L M" sort="Mokhova, L M" uniqKey="Mokhova L" first="L. M." last="Mokhova">L. M. Mokhova</name></author><author wicri:is="90%"><name sortKey="Bazarova, V B" sort="Bazarova, V B" uniqKey="Bazarova V" first="V. B." last="Bazarova">V. B. Bazarova</name><affiliation><mods:affiliation>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Sulerzhitsky, L D" sort="Sulerzhitsky, L D" uniqKey="Sulerzhitsky L" first="L. D." last="Sulerzhitsky">L. D. Sulerzhitsky</name><affiliation><mods:affiliation>Geological Institute of Russian Academy of Sciences, Moscow, Russia</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Lutaenko, K A" sort="Lutaenko, K A" uniqKey="Lutaenko K" first="K. A." last="Lutaenko">K. A. Lutaenko</name><affiliation><mods:affiliation>Institute of Marine Biology, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</mods:affiliation></affiliation></author></analytic><monogr></monogr><series><title level="j">The Holocene</title><idno type="ISSN">0959-6836</idno><idno type="eISSN">1477-0911</idno><imprint><publisher>Sage Publications</publisher><pubPlace>Sage CA: Thousand Oaks, CA</pubPlace><date type="published" when="2000-04">2000-04</date><biblScope unit="volume">10</biblScope><biblScope unit="issue">3</biblScope><biblScope unit="page" from="311">311</biblScope><biblScope unit="page" to="331">331</biblScope></imprint><idno type="ISSN">0959-6836</idno></series><idno type="istex">3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4</idno><idno type="DOI">10.1191/095968300667552216</idno><idno type="ArticleID">10.1191_095968300667552216</idno></biblStruct></sourceDesc><seriesStmt><idno type="ISSN">0959-6836</idno></seriesStmt></fileDesc><profileDesc><textClass></textClass><langUsage><language ident="en">en</language></langUsage></profileDesc></teiHeader><front><div type="abstract" xml:lang="en">Natural middle-and late-Holocene environmental development of Kunashiri Island reflects global climatic changes and the migration of warm and cold currents. Dry and cool climate changed to warm and moist about 7000–6500 BP, later than on Hokkaido Island. At this time Kuroshio Current system became more active. On Kunashir Island birch assemblages were replaced by cool-temperate broadleaf forests in the south and mixed coniferous/broadleaf forests in the north. The highest sea-level position reached 2.5–3 m above PSL about 6500–6300 BP. Cooling about 4700–4500 BP island vegetation weakly changed that connected with warm current influence. Major regression at this period led to formation of extensive coastal dunefields. The warming at the beginning of the late Holocene was almost similar to the Holocene Optimum. Two minor transgressions are recorded about 4010–3400 and 2950–2620 BP. Active entrance of detrital material to the coastal zone resulted in growth of accumulative landforms. Vegetation changes and climatic deterioration took place in the second half of the late Holocene. Coniferous and mixed coniferous/broadleaf forests shifted southward and occupied a large part of the island. During cooling at 1700–1300 BP the isthmus area increased, coastal wetlands with lakes and coastal dunes were formed, and grassland and swamp landscapes developed. Late-Holocene warming was not intensive. Active aeolian accumulation took place during the ‘Little Ice Age’ cooling and regression.</div></front></TEI><istex><corpusName>sage</corpusName><author><json:item><name>A. M. Korotky</name></json:item><json:item><name>N. G. Razjigaeva</name><affiliations><json:string>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</json:string></affiliations></json:item><json:item><name>T. A. Grebennikova</name></json:item><json:item><name>L. A. Ganzey</name></json:item><json:item><name>L. M. Mokhova</name></json:item><json:item><name>V. B. Bazarova</name><affiliations><json:string>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</json:string></affiliations></json:item><json:item><name>L. D. Sulerzhitsky</name><affiliations><json:string>Geological Institute of Russian Academy of Sciences, Moscow, Russia</json:string></affiliations></json:item><json:item><name>K. A. Lutaenko</name><affiliations><json:string>Institute of Marine Biology, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</json:string></affiliations></json:item></author><subject><json:item><lang><json:string>eng</json:string></lang><value>Island arc</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>environmental evolution</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>ancient shoreline</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>palaeolake</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>coastal dunes</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>palaeoclimate</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>sea-level oscillations</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>vegetation history</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>Kurile Islands</value></json:item></subject><articleId><json:string>10.1191_095968300667552216</json:string></articleId><language><json:string>eng</json:string></language><originalGenre><json:string>research-article</json:string></originalGenre><abstract>Natural middle-and late-Holocene environmental development of Kunashiri Island reflects global climatic changes and the migration of warm and cold currents. Dry and cool climate changed to warm and moist about 7000–6500 BP, later than on Hokkaido Island. At this time Kuroshio Current system became more active. On Kunashir Island birch assemblages were replaced by cool-temperate broadleaf forests in the south and mixed coniferous/broadleaf forests in the north. The highest sea-level position reached 2.5–3 m above PSL about 6500–6300 BP. Cooling about 4700–4500 BP island vegetation weakly changed that connected with warm current influence. Major regression at this period led to formation of extensive coastal dunefields. The warming at the beginning of the late Holocene was almost similar to the Holocene Optimum. Two minor transgressions are recorded about 4010–3400 and 2950–2620 BP. Active entrance of detrital material to the coastal zone resulted in growth of accumulative landforms. Vegetation changes and climatic deterioration took place in the second half of the late Holocene. Coniferous and mixed coniferous/broadleaf forests shifted southward and occupied a large part of the island. During cooling at 1700–1300 BP the isthmus area increased, coastal wetlands with lakes and coastal dunes were formed, and grassland and swamp landscapes developed. Late-Holocene warming was not intensive. Active aeolian accumulation took place during the ‘Little Ice Age’ cooling and regression.</abstract><qualityIndicators><score>7.616</score><pdfVersion>1.3</pdfVersion><pdfPageSize>516 x 768 pts</pdfPageSize><refBibsNative>true</refBibsNative><abstractCharCount>1499</abstractCharCount><pdfWordCount>9247</pdfWordCount><pdfCharCount>62133</pdfCharCount><pdfPageCount>21</pdfPageCount><abstractWordCount>218</abstractWordCount></qualityIndicators><title>Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific</title><refBibs><json:item><author><json:item><name>A.N. 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Dienst</title></host><title>Method of coding of ecological data from diatoms for computer utilization</title></json:item></refBibs><genre><json:string>research-article</json:string></genre><host><volume>10</volume><publisherId><json:string>HOL</json:string></publisherId><pages><last>331</last><first>311</first></pages><issn><json:string>0959-6836</json:string></issn><issue>3</issue><genre><json:string>journal</json:string></genre><language><json:string>unknown</json:string></language><eissn><json:string>1477-0911</json:string></eissn><title>The Holocene</title></host><categories><wos><json:string>science</json:string><json:string>geosciences, multidisciplinary</json:string><json:string>geography, physical</json:string></wos><scienceMetrix><json:string>natural sciences</json:string><json:string>earth & environmental sciences</json:string><json:string>paleontology</json:string></scienceMetrix></categories><publicationDate>2000</publicationDate><copyrightDate>2000</copyrightDate><doi><json:string>10.1191/095968300667552216</json:string></doi><id>3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4</id><score>1</score><fulltext><json:item><extension>pdf</extension><original>true</original><mimetype>application/pdf</mimetype><uri>https://api.istex.fr/document/3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4/fulltext/pdf</uri></json:item><json:item><extension>zip</extension><original>false</original><mimetype>application/zip</mimetype><uri>https://api.istex.fr/document/3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4/fulltext/zip</uri></json:item><istex:fulltextTEI uri="https://api.istex.fr/document/3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4/fulltext/tei"><teiHeader><fileDesc><titleStmt><title level="a" type="main" xml:lang="en">Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific</title></titleStmt><publicationStmt><authority>ISTEX</authority><publisher>Sage Publications</publisher><pubPlace>Sage CA: Thousand Oaks, CA</pubPlace><availability><p>SAGE</p></availability><date>2000</date></publicationStmt><sourceDesc><biblStruct type="inbook"><analytic><title level="a" type="main" xml:lang="en">Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific</title><author xml:id="author-1"><persName><forename type="first">A. M.</forename><surname>Korotky</surname></persName></author><author xml:id="author-2"><persName><forename type="first">N. G.</forename><surname>Razjigaeva</surname></persName><affiliation>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</affiliation></author><author xml:id="author-3"><persName><forename type="first">T. A.</forename><surname>Grebennikova</surname></persName></author><author xml:id="author-4"><persName><forename type="first">L. A.</forename><surname>Ganzey</surname></persName></author><author xml:id="author-5"><persName><forename type="first">L. M.</forename><surname>Mokhova</surname></persName></author><author xml:id="author-6"><persName><forename type="first">V. B.</forename><surname>Bazarova</surname></persName><affiliation>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</affiliation></author><author xml:id="author-7"><persName><forename type="first">L. D.</forename><surname>Sulerzhitsky</surname></persName><affiliation>Geological Institute of Russian Academy of Sciences, Moscow, Russia</affiliation></author><author xml:id="author-8"><persName><forename type="first">K. A.</forename><surname>Lutaenko</surname></persName><affiliation>Institute of Marine Biology, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</affiliation></author></analytic><monogr><title level="j">The Holocene</title><idno type="pISSN">0959-6836</idno><idno type="eISSN">1477-0911</idno><imprint><publisher>Sage Publications</publisher><pubPlace>Sage CA: Thousand Oaks, CA</pubPlace><date type="published" when="2000-04"></date><biblScope unit="volume">10</biblScope><biblScope unit="issue">3</biblScope><biblScope unit="page" from="311">311</biblScope><biblScope unit="page" to="331">331</biblScope></imprint></monogr><idno type="istex">3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4</idno><idno type="DOI">10.1191/095968300667552216</idno><idno type="ArticleID">10.1191_095968300667552216</idno></biblStruct></sourceDesc></fileDesc><profileDesc><creation><date>2000</date></creation><langUsage><language ident="en">en</language></langUsage><abstract xml:lang="en"><p>Natural middle-and late-Holocene environmental development of Kunashiri Island reflects global climatic changes and the migration of warm and cold currents. Dry and cool climate changed to warm and moist about 7000–6500 BP, later than on Hokkaido Island. At this time Kuroshio Current system became more active. On Kunashir Island birch assemblages were replaced by cool-temperate broadleaf forests in the south and mixed coniferous/broadleaf forests in the north. The highest sea-level position reached 2.5–3 m above PSL about 6500–6300 BP. Cooling about 4700–4500 BP island vegetation weakly changed that connected with warm current influence. Major regression at this period led to formation of extensive coastal dunefields. The warming at the beginning of the late Holocene was almost similar to the Holocene Optimum. Two minor transgressions are recorded about 4010–3400 and 2950–2620 BP. Active entrance of detrital material to the coastal zone resulted in growth of accumulative landforms. Vegetation changes and climatic deterioration took place in the second half of the late Holocene. Coniferous and mixed coniferous/broadleaf forests shifted southward and occupied a large part of the island. During cooling at 1700–1300 BP the isthmus area increased, coastal wetlands with lakes and coastal dunes were formed, and grassland and swamp landscapes developed. Late-Holocene warming was not intensive. Active aeolian accumulation took place during the ‘Little Ice Age’ cooling and regression.</p></abstract><textClass><keywords scheme="keyword"><list><head>keywords</head><item><term>Island arc</term></item><item><term>environmental evolution</term></item><item><term>ancient shoreline</term></item><item><term>palaeolake</term></item><item><term>coastal dunes</term></item><item><term>palaeoclimate</term></item><item><term>sea-level oscillations</term></item><item><term>vegetation history</term></item><item><term>Kurile Islands</term></item></list></keywords></textClass></profileDesc><revisionDesc><change when="2000-04">Published</change></revisionDesc></teiHeader></istex:fulltextTEI><json:item><extension>txt</extension><original>false</original><mimetype>text/plain</mimetype><uri>https://api.istex.fr/document/3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4/fulltext/txt</uri></json:item></fulltext><metadata><istex:metadataXml wicri:clean="corpus sage not found" wicri:toSee="no header"><istex:xmlDeclaration>version="1.0" encoding="UTF-8"</istex:xmlDeclaration><istex:docType PUBLIC="-//NLM//DTD Journal Publishing DTD v2.3 20070202//EN" URI="journalpublishing.dtd" name="istex:docType"></istex:docType><istex:document><article article-type="research-article" dtd-version="2.3" xml:lang="EN"><front><journal-meta><journal-id journal-id-type="hwp">sphol</journal-id><journal-id journal-id-type="publisher-id">HOL</journal-id><journal-title>The Holocene</journal-title><issn pub-type="ppub">0959-6836</issn><publisher><publisher-name>Sage Publications</publisher-name><publisher-loc>Sage CA: Thousand Oaks, CA</publisher-loc></publisher></journal-meta><article-meta><article-id pub-id-type="doi">10.1191/095968300667552216</article-id><article-id pub-id-type="publisher-id">10.1191_095968300667552216</article-id><article-categories><subj-group subj-group-type="heading"><subject>Articles</subject></subj-group></article-categories><title-group><article-title>Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific</article-title></title-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Korotky</surname><given-names>A. M.</given-names></name></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Razjigaeva</surname><given-names>N. G.</given-names></name><aff>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Grebennikova</surname><given-names>T. A.</given-names></name></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Ganzey</surname><given-names>L. A.</given-names></name></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Mokhova</surname><given-names>L. M.</given-names></name></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Bazarova</surname><given-names>V. B.</given-names></name><aff>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Sulerzhitsky</surname><given-names>L. D.</given-names></name><aff>Geological Institute of Russian Academy of Sciences, Moscow, Russia</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Lutaenko</surname><given-names>K. A.</given-names></name><aff>Institute of Marine Biology, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</aff></contrib></contrib-group><pub-date pub-type="ppub"><month>04</month><year>2000</year></pub-date><volume>10</volume><issue>3</issue><fpage>311</fpage><lpage>331</lpage><abstract><p>Natural middle-and late-Holocene environmental development of Kunashiri Island reflects global climatic changes and the migration of warm and cold currents. Dry and cool climate changed to warm and moist about 7000–6500 BP, later than on Hokkaido Island. At this time Kuroshio Current system became more active. On Kunashir Island birch assemblages were replaced by cool-temperate broadleaf forests in the south and mixed coniferous/broadleaf forests in the north. The highest sea-level position reached 2.5–3 m above PSL about 6500–6300 BP. Cooling about 4700–4500 BP island vegetation weakly changed that connected with warm current influence. Major regression at this period led to formation of extensive coastal dunefields. The warming at the beginning of the late Holocene was almost similar to the Holocene Optimum. Two minor transgressions are recorded about 4010–3400 and 2950–2620 BP. Active entrance of detrital material to the coastal zone resulted in growth of accumulative landforms. Vegetation changes and climatic deterioration took place in the second half of the late Holocene. Coniferous and mixed coniferous/broadleaf forests shifted southward and occupied a large part of the island. During cooling at 1700–1300 BP the isthmus area increased, coastal wetlands with lakes and coastal dunes were formed, and grassland and swamp landscapes developed. Late-Holocene warming was not intensive. Active aeolian accumulation took place during the ‘Little Ice Age’ cooling and regression.</p></abstract><kwd-group><kwd>Island arc</kwd><kwd>environmental evolution</kwd><kwd>ancient shoreline</kwd><kwd>palaeolake</kwd><kwd>coastal dunes</kwd><kwd>palaeoclimate</kwd><kwd>sea-level oscillations</kwd><kwd>vegetation history</kwd><kwd>Kurile Islands</kwd></kwd-group><custom-meta-wrap><custom-meta xlink:type="simple"><meta-name>sagemeta-type</meta-name><meta-value>Journal Article</meta-value></custom-meta><custom-meta xlink:type="simple"><meta-name>search-text</meta-name><meta-value> 'The H-olocene 10,3 (2000) pp. 311-331 Middle- and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific A.M. Korotky,' N.G. Razjigaevaj' T.A. Grebennikova, L.A. Ganzey,' L.M. Mokhova,l V.B. Bazarova2' L.D. Sulerzhitsk y2 and K.A. Lutaenko3 (Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia; 2Geological Institute of Russian Academy of Sciences, Ml1oscow, Russia; 3Institute of Marine Biologv, Far East Branch of Russian Academy (of ciences, Vladivostok, Russia) Receivled 20 March 1998; reviied manuscript accepted 10 August 1999 Abstract: Natural naiddle- and late-Hlolocene environmental development of Kunashiri Island reflects global cliniatic changes and the migration of warm and cold currents. Dry and cool climate changed to warm and moist aboUt 7000-o5QO BP, later than onl Hokkaido Island. At i5s time Kuroshio Current system becamne imore active. On Kunashir Island birch assemblages were replaced by cool-temnperate broadleaf forests in the south antd mixed coniferots/broatdlea'ftbrests in the nordt. The highest sea-level position reached 2.5 -3 m above PSL about 6500-6300 BP, Cooling about 4700-4500 BP island vegetation weakly changed that connected with { X.:: . s.....warm crrent influence. Major regression at this period led to formation of extensive coastal dunefields. The warming at the beginning of the late Holocene was almost similar to the Holocene Optiiurru . Two minor transgressions are recorded abotLt 4010-3400 and 2950-2620 BP, Active entrance of detrital material to the coastal zone resulted in growth of accumulative landforms. Vegetation changes and climatic deterioration took A place ia the second half of the late Holocene. Coniferouts and mixed coniferous/broadleaf frests shifted south- HOLOCENE ward and occupied a large part of the island. During cooling at 1700-13(00 BP the 'sthmus area imcreased. RESEARCH coastal ssetlands with lakes and coastal dunes were formed, and grassland and swamp lanidscapes developed. PAPER ILate-Holtocene ;warming was not intensive, Active aeolian accumulation took place during, thle 'Little Ice Age' cooling and regression. Key words. Iland arc, ensvironmental evolution, ancient shoreline. palaeolake, coastal dunes, palaeoclimate. sea-level oscillations, vegetation history, Kurile lsiands. Introduction The studv of middle- and late-Holocene environments is of inter- est for evolution of island geosystens within a background of' global climatic svarming as represented by the Holocene climatic optimum for the coasts of the western Pacific marginal seas and Japanese islands (Korotky and Khudyakov, 1990; Ktlakov, 1973; Sakaguchi, 1983). Preliminary investigations of the H1olocene ter- race sequences of the Kurile Islands were made by Aleksandrova (1971), Melekestsev et al. (1974) and Bulgakov (1993; 1996). Deposits representing a Holocene climatic optimum were first fotmd in los marine and lacustrtme terrace secuences of Kimashir (Korotky e aL., 1995). T'his paper presents new stratigraphic data for Holocene deposits of Kuniash.'ir, which .allow us to reconstruct enviromnental and climatic changes in more detail. The strati- r.) Ariold 2000 graphic study of Holocene sequences tecuses on environmental reconstruction in tesponse to such factors as regional clirnate, sea- level fluctuations, the migration of warmi and cold currents and volcanic impact on the environrnient. Regional setting Kunashir Island (43'40'-A4430'N, 145"23'-46030'E) is the larg- est south. island of Kurile Island Are, stretching froim So-uth Kam- chatk.a to Hokkaido Isltatd. 17.mena Strait (15.5 km wide) divides Kuiashiri from n-ortheastern Hokkaido (Figure 1). Kitnashir Island is about 123 km long, 7 to 35 km wide, and 1490 kma in area. The Pacific Ocean borders the island orn the east and the Sea of Okhotsk on thle west. KIuiashir Island is situated along a zone of 0959-6836(00)1H1L392RP 312 The Holocene 10 (2000) - --*- - -- -- -- -- -- -- -- -- -- -- -- -- --- - - -- - -- - - -- --- - - - -- -- - -- - - - -- - -- - - -- -- - -- - - -- -- -- -- -- -- -- -- -- -- -- - - - Kunashir AN I~~~~~~~~~~~~sland + N J/ a~~/ Okhotsk Sea /c imn.ac-n.anMkav2 a v ne ttr, u ar ; ,$+;14 -~lAt.,T ,-'str 7A .11 e Las~~~~~~~ iss~~hn Ls J | olceno y~ t\ / f Ocean >,o~~ovssi g ~ ~ ''~~~~~~~~ -47-------TF37-s---X------- - --------- -- -- ---- ______-______ _ = _ ______ H s :sh id s ) v, noden saumple A outcrups Figure I Location of the study area. convergence of two adjoining plates where t, e Pacific plate sub- ducts under the Eurasian plate (Sakaguchi. 1980). The fact that Kurnashir Island is located on a subduction-type mobile belt explains the intensive seismic and volcanic activity here. Kiinashir Island exhibits mountain relief (Up to 500 -1800 m) resulting from th.ree volcanic groups and three low isthmuses (from 2- 5 m to 25 m high). Rluruy and Tyatya Volcanoes are active in the noorth and Mendeleev and (Golovnin Volcanoes in the south (Figure 1). Dokuchaev Ridge, composed of Neogene vol- canic rocks and granodiorite intrusions, occupies the middle part of the island (Gorshkov, 1967). The Quaternary deposits consist substantially of volcanic, fluvio-lacustrine and tnarine sediments, which lie unconformably on Neogene sequences. Late-Pliocene/ Middle-Pleistocene marine deposits comprising the south part of thfe islands were consolidated to form the Golovnin Formation (PryaliAI3uina, 1961; Pushkar et at, 1996). The Upper Pleistocene is composed of a variety of terrestrial alluvial, lacuStrine, vo1canic .and aeolian sediments. The climate of Kunashir Island is strongly influenced by the Asian Monsoon. Duringg the winter the northwest air masses from Asia produce severe cold and snow. Dutring the summer moist cool Pacific air masses move souatl or east across the Kurile Islands toward the Asian low-pressure area, bringing with them extensive rainfall, fog and typhoons in August--September. Mean annual tempeatLure is about 4.7WC (Atlas of Sakhalin District, 1967: Reference Book of USSR Climate, 197(i). Jantuary mean temperature is about -5-.6WC. A-ugust mean temperature is aebout 15-16W. and summer temperatures can reach 32.1 tC. Annual rainfall is about 1040 nmn. Ocean currents are particularly important in influencing the regional climate of the Southern Kur- ile Islands. The warm Soya current is most important, as it has a warming effect on the southern part of the Sea of Okhotsk. The Oyashi'o cold current brings cold water from north to south in the Kurile region. The warm Kuroshio Current produces synoptic eddies (Kamenkovich e a!., 1.987), which in.fluence the southern part of the island. Marine currents, mountain relief and hot springs define a wide range of microclimatic conditions and a high diversity of ecotypes (A.Qekseeva. 1983). The vegetation period on the Sea of Ok(hotsk side is warmer than o -the Pacific coast. Phenological data Show that plants on the O1k.hotsk side develop earlier than on the Pacific side, and the sanle phases of plant development begin 8-10 days earlier. This is explained by the influence of the warm Soya cur- rent and by the barrier role of the molunain reliet, protected from fog and cold winters caused by cold water of the Oyashin cutrren-t (Vorobiev, 1963). The moist climate, wide latitudinal range and mountain relief combine to produce two botanical formations on Kunashir Island (Alekseeva, 1983, Vorobiev, 1963). Cool-temper- ate broadleaf and mixed coniferous-broadleaf forests of the Nemurno-KurAshiri Formation occupy the southern part of Thde island. Broad-leaved taxa inrclude Quercvs crispula, Q. denrtala, Acer pictrm and A. ukurunduense in association with Kahpc'anax seprtemiobum, Phellodendron sachaliense, Cerasns' sachal/nensis. C. maxrimoiviczii, Ulmus lacin/tsa and U propinqua. Conifers are represented are represented by Ahftes vachalinensis, Picea microsperrna. P. glehnii and Tax.rs cu tspdata. Such thernmophyl- ous species as Magnolia obovoata, Bernia Afaxrnowicziana, Alnus japonica, Fraxinus manshurica, Svringa amurensis; Act/nidia argulaa Botracr/urm conta-oversum and somie others are found only in this southern part of the Kurtle Islands. Boreal coniferous forests of the Kunashiri-It-urup Formation with dominant Afies sachalienensis are extensively distribiuted in northern Kunashir. The boundary between these two vegetation formations is located in the central part of the island. Grassland develops on lzmena Bay coast on the soudi and on Lovrtsov Peninsula on the north. Six altitudinal vegetation zones are present onl the island (Aiekseeva. 1983; VY!orobiev, 1963): broadleaf forests zone (Up to 300-400 m in dte south and to 200-250 near Ruruy Volcano hot springs and withain river valleys in the -north); boreal coniferous forests zone (up to 500-700 m in central andi northern parts), Betrla ermani zone (frotn 400-600 m in the northern part); Pinus pzurila zone (fragtnenits in lower zones andiS Lip to 1 500 mi). heath zone-Ericaceae-Empetrum osiatiurn zone (fragments in lower zones); and alpine zone (Ruruy and Tyatya Volcanoes tops). One of the main landscape plants is Sasra on the lower and midadle slopes. Modern pollen assemblages reflect today's vegetation of the island (Table I). Arboreal pollen dominates near forests, and non- arboreal polle-tl and its diversity increase near grassland and peat- land areas. Coniferous pollen dominates in the central pa.n of the island, and to the south broad-leaved pollen increase. More thenn- ophilous taxa were found only in the southem part. A high content of A/ntus occurs near swamps and reflects river-valley forests. Material and methods The HIolocene sections studied include low manne and lacustrine terraces, wetlands and dunefields. Some outcrops were selected for detailed observations and sampling. Figure 1 shows the location of outcrops studied within low terrace sequences at 2 m elevation (site 5858), 3-4 m elevation (5822) and 5-6 in elevation (5706, 5705, 5815 arid 5936). The peat bog near Fedyashin Cape was sampled in 1994 (5871) and 1995 (6395). Diatom and pollen samples were analysed at 10 cm intervals from lacustrine, marine and peat units or at varying intervals dependinig on the sediment lithology. The pH values from deposits were measured irn Thte field. Modern pollen spectra from surface alluvial and lacusurine silty sands were studied for more correct interpretatio-n of fossil pol- len data. Diatom processing methods follow those of Gleser et al. (1974: A.M. Korotky et a!.: Veget ation history of Kunashir Island, Kurile Islands, northwestern Pacific 313 Table I Pollen data on modern alluvial and lacustrine sediments of Kunashir Island Location Filatov R. Prozrachniy SoLth Kurile Serebryanoe Serebryanka Khlebniko;v Temnaya R. Veslosskaya Stream isthmus, L. R. Stream Spit stream Total counted Arboreal pollen Nonarboreal pollen Spores A-rboreal pollen Abies Picea sect. Omorica Picen sect. Eupicea Pima.v s/g Haploxylon Betvula sect. A//ae Bentla sect. Cawatae Beula sP. Reta/a seCt. Nuin ae R1eti Ia; e'iiis Berla/ middenezdorffii A/ naster Myrica /mits Qiuercus Jug/aru Ze/kova Coryius c'arpiu.;s Pheflod/enLdron Syringa Rhus Viburnum Norarboreaa pollen Cyperaceae Gramineae (ompositac Artemiia Umbeiliferae Ranunculaceae Rcmwvicuhuc Ericaccae Saxifragaceae Rosaceae Tha/ictrum San-uisorba Piranavgeton T;'rj pha Caryt phyllaceae Chlenopodiaceac Fobaceae Cryacifera Po/vgonuil R.tbaceae Varia Spores: Polypodiaceae Pa/ypOdium vI/ligare Polypodliun dirya,,teris Omununda Lvcopadivm all/pnuiat Lycopodium c/avatunm I yc( op)od/am comp/anatum lvl oec/tam .Se/ago) Lvapadium /)uigens L cafepodi/un I.. annoliur .St/haguian Equisetum 573 37x 18 ,17 320 27xR 3 39 80 20 [4 4 13 4 43 36 109 77 2 9 10 33 66 3 I1 1673 769 146 758 210 290 40) 10 52 I? 6 4 120 2 444 329 62 53 99 121 6 331 22 7 I1 24 16 4 1177 655 356 166 170 210 7 11 33 51 734 397 184 153 90 130 12 3 10 4 685 323 204 158 301 202 43 56 22 60 9 70 21 9 18 21 2 4 4 7 11 31 46 50 100 31 21 61) 64 ?7 10 6 2 6 4 13 1 5f6 6 2 24 21 2 3 2 1 2 33 43 31 70 11 6 21 3 3 1 70 so 2 6 ., 2 40 ll 25 150) 34 267 36 3 2 I 3 1 2. 6 20 172 160 60, 79 4 13 34 11 6 4 20 14 10 4 34 13 69 102 6 6 31 31 '7 l 34 11 3 20 15 90) 2 2 1 8 12 19 50 1 1 .cO 9 3.4 2 3 8 'A 21 3 4 11 44 124 32 3 24 4 2 8 4 12? I1 t 10 I I I I I 314 The Holocene 10 (2000) 55-79). The samples were treated with a solution of hydrogen peroxtde and washed with distilled water. For certain diatom prep- arations heavy-liquid (mnixture of 1-120:CoJa:KI = 1:1.5:2.25, den- sity 2.4 g/sm3) was used. Permanent preparations were made with 1 8 x 18 mm ecover galases and Plyashev anil inc-formaldehyde resin with refraction indices n = 1.66-1.68. Diatous were ident- ified at magnification xl 000. When possible, 200-300 valves were counted per sample. Tihe ,thanatocoenoses approximately 1eflect the taxonomic composition and ecological structure of recent dia- to-m commnunities in the uppermost water layer with specific eco- logical hiabitats. The ecological significance of diatomi species was taken from de Wolf '1982), Denis (1991), Krasmmer and Lange- Be-rtalot (1986; 1988. 1991a; 1991b), Jouse (1962), Davidova (1985) and Barinova and Medvedeva (1996). The ecological data provided by the above-mentioned authors has enabled most taxa to be grouped into the thlree categories marine, brackish and fresh- water, and then divided into planktonic and berthic species. Only taxa with the highest abundlance and important indicator species are graphed. The material for pollen analysis was treated by the standard KOH and acetolysts method. Pollen grains were concentrated by means of the heavy-liquid flotation method outlined by Pokrov- skaya (1966). More than 300 pollen anid spores were counted in rich samples. Three pollen sums were calculated: total arboreal pollen. total rnonarboreal pollen and total spores. Age wcas determined by 14C analysis and teplrostratigraphy. 'S dating of the samples was obtained on wood anid on pe.at samplt.es 10-20 cma thick. The samples were treated with standard acid and ;alkali sohluions. 4C dates were produced by liquid scintillation colrting in the Geological Institute, Russian Academy of Sciences, Moscow. Full ' C age data Ifr deposits of Kumashir Istand were published by Bazarovta et al. (1998). Table 2 lists the ;4C- dates for the sections studied. Tephra layers were identified in dte field and later studied i n the laborator' umder cross-polarized light. For mineral analysis, the 0.05-0.1 mm and 0. 0---O.25 mm fractions were separated from tie sediment samples by wet sieving. H-leavy minerals were extracted with tribromomethane (density 2.89 g/sm3). The cheini- cal (wet chemistry) composition of ash layers was also investi- gated. The correlation of ash layers is based on '4C dates floiln under- and overlying deposits, on refractive indices and mor- phology of volcanic glass shards, and Onl chemical and Mineral composition. Results and interpretations Middle-Holocene deposits Tae deposits correlated with the Ilolocene optimum are found on the Pacific coast in Kosmodemian.skaya Inlet (sit&es 5815, 57706, 5705). on the middle part of Serebryanka River (5822), ot, the lower part of the Lesnaya River (5936); o-n the Okhotsk Sea coast at the eastern side of Lagun~noe Lake (5801) and at the peat bog near Fedyaslin Cape (58711). and on dte. Ilzmena Bay coast near the Khletnikov Stream tmouth (5858). Kosmodemyanskaya Inlet This is the most northern point investigatied. The 5-6 m terrace there is composed of different facies (Figure 2). Lacutsuine deposits are exposed at the base of the terrace. Stratigraphy of 5705 ( and 5706 was published (Korotky et at., 1995). Here we report the results of the study of 5815. located in the back side of thne terrace, where the deposits of the peripheral pat of the palacolake are exposed. The deposits contain rich freshw-ater dia- tom assemblages typical of small lakes (FiguLe 3). The diatom composition reflects stages of palaeolake development, Blue-grey silt with abmndant remains of water plants (2.7- 3.1 ni) fron the base of this terrace at site 5815 include bottomIn Table 2 '4C age data of Holocene deposits of Kunashiri Island Sample no. Collection site Position Depth (ml) Material '4C age (yr BP) GIN-no. 1,5815 Kosnodemianskaya Inlet 5--6 m terrace 2.0G-2.15 Peat 5240 I 50 8337 11/5815 Kosrnodemianskaya Inlet 5-6 rn terrace 2.40-2.45 Peat 5800 ± 70 8336 11115815 Kosmodemianskaya Inlet 5-6 m terrace 2.80-3.00 Wood 6460 ± 100 8335 1/5813 Kosmodemiatnskaya Inlet 5--6 n terrace 200 2.20 Wood 4560± 150 8338 J1/x5 13 Kosinodernianskaya Inlet 5-6 m terrace 2.00-2.20 Peat 4780 ± 1l00 833 1/5822 Serebryanka River 3 --4 mn terrace 0. 6 Wood 80 ± 50 8429 11/5822 Serebryanka River 3-4. e terrace 0.7-0.85 Peat 600 ± 6O 8627 1 1/5 22 Serebryanka River 3-4 m. terrace 0.7 Wood 10 ±40 8341 fv/~S2) Serebryanka River 3--4 r terrace 1.00-1.20 Peat 1960 ± 80 84301 V/'5822 Serebrvanka River 3-4 m terrace 1.30-1.40 Wood 2780 ± 60 8431 V1/5822 Serebryanka River 3--4 m terrace 2.10-2.20 Shells 5,0201+ 100 8433 VIJ/5822 Serebryanka River river bottomi Shell s 5620.± 100 8432 a b 1/.536 Lesnaya River 5- 6mn terrace l1S-41.65 Peat 4260160 8435 11/6936 1esnaya River 5 --6 n terrace 1.75 -1.90 Peat 4970 ± 80 8436 111/5936 Lesnaya River 5- m. terrace 2.50 -2.55 Peat 5750 ± 100 8437 IV/5 936 Lessnaya River 5 -6 rn terrace 2.10--2.2( Wood 5410 ± 40 8344 V/5936 Lesnaya River 5-6 e terrace 4.10-4.15 Peat 6440 ± 100 8438 1/5 87 1 Fedyashin Cape Peat bog 1.4)- 1.50 Peat 41(00 50 8333 JI1/5s 1 Fedyashin Cape Peat bog 3.00-3.1 0 Wood 50001 70 83 34 1/6'395 liedyvashin Cape Peat bog 0.60--0.7t) Peat 3960 ± 50 8948 lW/639i Fedyashin Cape Peat bog 1.90 ---2.00 Peaty silt 5900 I 40 4949 V/bt-395 Fedyashin Cape Peat bog 2.00-2.20 Peaty silt 7910 ± 140) 8950 1/5858 Khlebnikov Stream 2 mn terrace 0.35-0.42 Peat 2?070 ± 3(0 8440 115S58 Kbiecbnikov Stream 2 m terrace 0.46-0.58 Peat 2080 ± 80 8441 111/5858 Khebnikov Stream 2 m terrace 0.46--0).55 Peat 2730 ± 60 8442 fV/5858 KhIebnikov Stream 2 m terrace 0.65 -0.75 Peat 3790 ± 70 8443 V'/5858 Khbebnikov Stream 2 m terrace 1.30-1.40 Peat 461)00)±70 8343 t/5891 Vodopadny Cape Bench 041.0t Peat 851 ± 50 8428 1/(5801 Lagiinnoe Lake terrace 1.9 2.0 Peat 65201 0o 8340 A.M. Korotky et al.: Vegetation history of Kurnashir Island, Kurile Islands. northwestern Pacific 315 E ~ ~ ~ ~ ~~ ~ ~~~~~~~~~~~~~~~~ 5224 D - SG u' ~~~~~~~~~~~~~~~~~~~~~~St ' I rn 41., )4-7-i ~ ~~~~~~~~~6460 I100, .r,.S 44s~~~~ti1-;itl ~rr d 4 7eh' 1qz S ,.s tn' 4 'lsc 5 79 - 2620-.9C 50 L'Vt I 5706d '',utcr(-,, 'iiQ. '0o , 9(1 d . - ... 2 1 4s:: 4 4 45 7 L-, / 0 592Ln 50) o ; 5 S'b5 outcop I. * lMu- c 2'= 4x,5 6 C' 5 4 78L I . 4:C5 5a 1 5 ou'crou m n7 ,: v;: MU-b 1 - 2 5 2 40C ±00 3 ., L _ .O 3 0- 40"-l 100 EIx::3 pl xrai kp, = sii = sand =grow F olWX-;-osand bbis s (Eisr etils Lt.._-_wen W .-p-la [3pcrnirt - J ash TjFeerudlrOS:°P Figure 2 Cross-section of 5-6 m terraces of Kosmodemyanskaya Inlet. Q2.v = middle HIolocene; Q3, = late Holocene. Facies: m = marine. e = aeolian. species and epiphytes (Dip/oneis elliptica up to 19%, D. ova//s up to 4%. Funoria praerupra) and plankton (A4ulacoseira granul- oM LIp to 12%,. A. ait/ica oup to 20%, Diatooia hyemal/sv tip to 7%), which indicate a flooded hake environment (Korotky e al., 1988; Bari nova and Medvedeva. 1996). A pollen assenmblage with domii- nance of Ben/a sect. Nanae (up to 55%1o), Betu/a sp. pup to 18%1) and A/naster (up to 300/0) (Figure 4) indicates a cold climate and park-tundra landscape. The deposits could be correlated with the, Last Glacial Stage. but the '4C dlate of 6460 t 100 BP, obtained from wood, does not support +this correlation. This vegetation type was representative only of lateglacial environments of the land- bridge area between Ku-nashir and Hokkaido Islands (Tsukada, 1-986). Above the basal silt is interbedded peat and peaty silt with thin horizontal laminations and rare sand layers (1.7 --2.7 mtri. The basal peat 42.6-2 7 -n) of this Unit is characterized by a high content of P/emu/ar/a lata (up to 38%Sl), P. noNilis (up to 16%). Eunostia pra- eru'pta (up to 24%) and U[ant.seh/a amphioxys (up to 3%), which indicate the swamp margin of the palaeolake (Davidova, 1985; Barinova and Medvedeva, 1996). Above this (2.4-2.6 rn) epi- phytes Fragi/aria construens v. venter (up to 34%), F. pinnata (up to 230/c.) andF brevi'iri/ta (up to 54%) dominate. The pollen assemblage fro-m the peat (2.3-2.7 m) has a dominance of broad- leaved gonera (Quereus up to 59%, Juglans up to 15%',°', P/elloden- dron up to 3%, U/nlms up to 4.8%. Acer and Syringa), reflecting the distribution of cool-temriperate broadleaf forests. The deposits are (iated 5800 ± 70 BP, A sharp increase of Alnaster (28%) and Bettl/a sect. ANanae (10%) (in the interval 2.2-2.25 mn) reflects a weak cooling wvithin the Ilolocene optimum. Peaty silt (2. 1 -2.4 mn) contains lacustrine dliatom assemblage of epiphytes (Cocconeisv placentula up to 19%, Achnanshes tanceol- ta up to 20%/O and Epith/mia zeb:ra LIp to 17%os;) and a high content of planktonic A4ulaeose/ra granuifwa (up to 25%,.,). Pollen of Quercus (up to 50%/c) with other broad-leavedi taxa (.Juglans up to 100/c, ULitus up to 10%X0, Aralia, Phellodendron, Carpinus) plays a pnimary role in the pollen assemblage. The deposits were dated at 5240 50 BP. The top of the peat (1.75--2.1 m) contains a diatom. assemLblage with predominanice of benthic Pinnuloria virdids (LIp to 115%)j P. .strueptoraphe (ulp to 74), P. brevicostara (up to 10%)', P. major (up to 15°/c). P. nob/i/.s (up to 1]5%), P. boreahus (up to 6%) and Dip/onteis ovals (up to 34%Xo), which. intdicates swamping ofthe lake. Pollen assemblages contain mainly Qzuercuxs, and the diver- sity of the other broad-leaved taxa decreases, reflecting the devel- opment of oak forests. '4C dates from the top of the peat dates are 4560 ± 50 BP and 4780 ± 1 00 BP. Serebryanka River Middle-Holocene deposits are found on the Pacific side of the South Kurile Isthmlnus within a low peatland (up to 6-7 m height) with a series of well-pronounced storm ridges, repeating the con- tour of the South Kurile Inlet. Figlure 5 shows cross-sections of this peatland. The investigated section is located on the left side of the Serebryanka River about 2.5 'km fronm the nmouth within the large storm ridge with a coniferous forest (5822). Somie shells of marine molluscs were collected here in. the river, including Cras- sostrea gigas (Thunberig), Rudit/apes phi/ippitarum (Adarms et Reev), Alacoma inconigrua (Martens) and Mya japun/ca Jay. The similar mollusc assemblage indicates sublittoral zone of opened bay with sand bottom. Two ''C dates on shells of different mol- lusc species have identical value 5620 ± 100 BP. The base of site 5822 exposes blue-grey coarse sandi (1.9- 2.2 m) with molluscs, including A'va japonica Jay and Ruditapes philippinarum (Adamis et Reeve), typical for semi-open bay. The 14C date of shells (50'0 + 100 BP) suggests that t'he toznbolo dividing, South Kisrile and Giolovnin Inlets was fonned by them. The sand includes rare marine diatom Paralia sulcota, and A ct/io- evceus octonarius and freshwater Cvymbe/la sinuara, Diplotte/s ovalis and Frustulia rhomboides (Figure 6). The pollen assem- blage (Figure 7) reflects die distribution of cool-temperate broad- leaf forest with Quercus (450%), Ulmus (2%) and Juglant (1.4%1E) and small amounts of small-leaved genera. The climniate was warmer than the presenrt, because modernl pollen spectra of this area are composed of mainly conifers (to 78%) and birch (to 13%). Lagoon Lake On the Okhotsk Sea side of South Kurile Isthlumus a mniddle- IHolocene lagoon unit (up to 0.15 mn thick) was found or. the east- em coast of the Lagoon Lake (5801). The elevation of this lagoon unit is 1.2 m higher thean modem lake level. Trhe deposits are rep- resented by well-rounded boulders with sandy matrix and peaty sand. The &atom ,assemblage includes marine Paralia, vs/cons, Cvc/otela striata, Actinocyclus octonzari/v and T/sa/assios/ra 316 The Holocene 10 (2(0(0) o 0j ..3. c_ $ n - set~oqpess /of14w/ D~jnjflJni& DJ/esSC'30/f su130q Jc D4dni;eod pl40oJn SI/OAC) .feuc)/c!/ SAXCiL/dLUtD L)!USCZ:4LID wu4XAl,1 I - co -t3 _o C t -,) D4DSOQJAQojq Jr,.LLJ O1IC70U 0(4dqDJ.0JCAS S1.J74J,'A 0110/fl Li'), sOp,,. Lun,,pl o 04DJDSGUG; oplcaqrq n nidnd * ,V4OICe;9StUijQ, L-j.-JC7.)( DIUpIo DtJ~E1ic fSuoui DA JfliD/!'C4JLe( 0/¶Jg41A4Jq ,'i[@/'J ^CZQ4~lOUU~d ?3 __~___ ____ _ ft_]WSL_ IULJ I t '3 L ~Of M. H , .4L 4 + &------------------ .--. . ~S 't- II -4-JJ -i| a + nulllnS 1loltll+-dt. .p, d~~~~~~~~~~~~~~a .... . . . --------------__h PI N, _ _ _ - 4 i-. . .d u lEll iLq- - ; 3 J.I1n n- pli-JJ N4 _ _ _ _ _ _4 _ ------------------------- ----- - - ~~~~'- -ln" -- -- - - - - - - - - -- - - - - - - - -- - - - - - - -- -- - -- - - - -- -- 4- -- -- - -- -- - - ------------ la-j M Ala , ________------------- ------ ------ ---------- ----- --- -F ------- J J :;;>,~~~~~~~~~~~~-------- ' ' S1 4- 0] .I- l c--i VI +I SU~ .)j/5k,{A JO ,, ;, I Pe q A /z.s JJ 0/16 C j + _ '. . t AueA q O w o ~D ,c _ _ _ _ _ _ _ _ _ _ _ _ _ _- ! - 4- 4-~ ~ ~ 4- 6 6, + CC r ( t )-~ K.1j-. .t j K -i44 IK@ (U.)) 77, k-I .P i, : 4 ;.%4 ,j O 9 VI 4. r: ._ E. E 0._ Li't' i .1 rGuel')! S?Ijiou A.M. Korotky et a!.. Vegetation history of Kunashir Island, Kurile Islands. northwestern Pacific 317 seaboqwessV uanpDOdcDA7 wnuotpqo'dS ;o>r. (qoq{pc~dSod aDGoP#At!(oAJD) )L3or-).n 0 r, uod oznoufltirt07, 0)ogsodN.)o oosouluuo *IJ/LU019 ucu~p-epol° snpJlc SI OOUIDN I4005 -0110a CIS C1T),1043 eoipgDo0- 'pZXS 41rLE; oovcb1 is Q.0Ok L)QPAWON 5/S SYEOld ooqidn.3 pos O>~ rO ./o) I -10W ) S C1-9!d qJOH uellod sqrnqs pU'J s9904 q1uilI H n J n.-n 1 -------------0------------ 4 , + - 'I n I : f i I : t gl I F I q 1 1 - 9 i H I I I± _-_ h-- 1L.. ri n nflftflnA L I -I l - ; iI* ~II I II 1 1 1 -----------------b~h- )1 n -- -- -- - ------ ------ n: anD~ ~ ~ ~ ~~~~Ii~ ____________________________ -,'. 1 t Ii 1 [1 + n 1jii t: air - . -_ _ I n + : ri- nnn, !; riF + +- 1 L _ _a . - --.- _ Ii+ _ -' + i + 1 -jl- l i Fl n ~ n rn . 1 . n + ,1 I I+ - 5In ------ k F,-- r - nt rn I "- ~l 1JLII nfl . .- A h i iF' I I II II rl I '1I11 itiiii III . I. Ii Cl C 04 C0) L I) (C) I I I II .4Ir, I II I II I 0 + O... ..4M,,-.K ,4 : :.L1-t 1Il4: I w) L4doI Cil ,) '11c tn .2 ^.c A.I as Z.. "i- 0 1i Ln C_ 0( et: + Vu 0 I= CoJ 1- R .2 q 01) r-) I.. i I 4-. iq . I ,: L I ! Is I , -s , . .- * , ..I!I i1I I n~~~~~~s~~~~~~gnor~~~~~~~~~~~~~~rs ~~~~~~~.i r 1l ,; 1 -- - - r _ . .1 -.. 1. H . .. . I § _g.s|i 4--- - ---- ---------- ii- F1 s - I SI !;r.- ---- -- -n ----- Li : I I I I i; I I I I I I I I -1 I 1R a I i I . I I i i i i II I ++ t+ +,t- nr- r-i + ---- Q. .9 n prl- GE 0 -u ------ ;-- ? i-I +F n + rl 64 318 The Holocene 10 (2000) Figure 5 Cross-section o01' eatlatid of Pacific side of South Kurile Istlhmius. hramapuwae. and freshwater LDiploneis ovali/, Gomphonema ace- minatiem, Novicula cryptoceph/w/. etc. A '4C date obtained from lagoon peat is 6520 ± 1 10 BP. Lesnaya River Middle-Holocene. deposits compose the 5-6 m lacuistrine terrace, located in the low cuirrent of the Iesnaya River and stretched 1 km along the river. Two sectiols of lacustrine deposits were studied: site 18 -93 exposes a peripheral part of the paleolake 250 m from the mouth (Korotky et aL., 19951, and 5936 exposes the deposits of the central part of the paleolake 800 m ftrom the -mouth (Figure 5). The deposits (site 5936) from the terrace base (2.55--4.2 m) are represented by light green-grey to dark blue and black clay with thir horizon tal and wavy laminations with sandy layers and vert-i- cal remains of water plants. The low value of p1-1 (4.2-6) indicates itnput of sulphuric-acid waters of Lesnaya River, resulting from Kisly Stream from Mendeleev Volcano. There are four diatom assemlblage in these deponsits (Figure 8). The oldest from die terrace base (4.0-4.2 m) inclfudes mainly epi- phytes Etinotia arcevs (up to 20%), E. tenella (up to 17%), Cacconeis placentutla (up to 8%) and C. placentula var. eeuglypta (up to 6%). and benithic Pinnu/aria interrupla (up to 3 )8%) and P. gi/'ha var. linearis (up to 6%), which indicleate the development of a small lake. 'The deposits were folmed abouit 6440 ± 100 BP. Maxima of planktonic Aulacoseira grane/lat (up to 75k5%) and A di.s!ans (up to 5%) from the interval 3.6--4.0 m indicate an increase of' lake. depth. Thie presence of marinec species typical 1br coastal regions (Od(/nte//a aurita, Trachyneiys aspera, Para/ia .se/1cota, Ta~as.avo.isira gravida) arrived in the lake with storm \waves, showing that sea level was higher than present. The third diatom assetnblage (3.0-3.6 rm) is similar to the first. Developmen.t of epiphytes Fenortia ar-u.s (ulp to 23%), .F. tenel/a (u.-p to 14%), E. valida (up to 7%/?) and Coccoaneis placenula (up to 10%), and benthic P/onelaria interrtqpta (up to 28%) and P. gibba var. tin- corns (up to 13%) are co.nnected wvith shallowing and swamping of te palacolake (Davidova, 1985). The fourth diatom assem- blage (2.55-3.0 in) with dominance of planaktonic Au/acoseira granua/ta (up to 50%) reflects a new pluvial phase btut without influenlce of stormi waves. The pollen assemblage (2.55--4.2 n-i is characterized by the dominance of broad-leaved genera wit-h high diversity (Figure 9): Quercwvs (23-56%), Juglans (5-10%), U/inzis (up to 36%,') and Phellodendron, Acer, Syringa, Fraxinus, Tilia, Fages. ('arpminus, Pierocarva, Aralia and Aconthopaniax. The assemblage reflects the development of cool-temperate broadleaf forests. The presence of Abies, Picea sect. Eupicea, P. sect. Omorica, .Pins s/g Haplox- ylon. Betula sect. Al/he, B. sect. Consatae indicate the develop- ment of coniferous and birch forests at higher elevations. The role of Alois (up to 22%) was great in valley forests. The climatic conditions were considerably warner than present. '4C dates are 6440± 100 PP for the base of the unit and 5750± 100 BP for ile top. The middle part of the section (1.9-2.55 m) exposes interbed- ded clay and peat. The diatom assemblage with high content of planktonic Autacoseira granutata (up to 20%), A. itol/ic (up to 27%,)t', and Stephanodiscus tot/a (up to 7%) indicates a pluvial phase of the palaeolake development. Alkaliphilous and alkali- biontic epiphytes predominate: Coccaneis placenteto (tip to 32%,/,), Diptloneis ova/is (up to 10%), Epfithemtia adc/ato (up to 1.5%) and Rhoplal/dia gibba (up to 6%). Pollen of sniall-leaved genera (Baeila sect. Costatae up to 8.8%,4,, B. sect. 41/he up to 23.2%/0, Antoes up to 16%,<,) and conifers (Pinltes rn/p Haploxylon up to 8.1%, P/cea sect. Eupicea up to 4.4%) increase in a background of broad-leaved taxa (Quercus 30.9%/o, Juglans 5.1%, Utens 2 .Q°%). Sharp decrease in quantity and diver- sity of broad-leaved tree pollen (Quercus 3.2%. U/roes O.3%, Jlg- tans 1I%) in the middle of die interval (Figure 9) rellects cooling and regession. High content of 4Ato.s (80.4%) indicates wide development of alder forests on the coast and along rivers at this time. The '4C date 5410 ± 40 BP for wood ftrom the top of this interval pennits places the cooling about 5.7- 5.4 ka BP. Dark blue clay with layers of greeni peat (1.65-1.9 m) includes I S ]t)! nra 1 . A.M. Korotky et a!.: Vegetation history of Kunashir Island, Kurile Islands. northwestern Pacific 319 s9eplq o'1o olcfn.exojd 3; DiIDf3}15 3 [ sypjou,,op~doo .sEpIszqLLco(4J Dj/r-~snJ~ J&JULA IDA SUL.erlJsuoo - suoeruguo0o A(.)!Jo.)IIOJJj Dl~OflJisus D//GqLJJAQ lO,.ffijo d Jo!ow (1)- (a) .e . . _ I a ~~~~=ol~ns oe'iordI E #5V,N@0JqueJq snoe~prouclooiV 1 C0 (wuj ti4dea ._ a), a4) M C t C) CZ I -o D C) .r E C) .W C V 1 1 rrl *- Fi ._ co ll~i,,--!,ri"~r l1. -14 1 1 1- - . I -- . %] | a i I . _ L I- I i II t 320 The Holocene 10 (2000) O V - - - - --~e ~ - --- - - - - - - - - - - - 7 - - - - - - - - - - - - 6-C?? ! p o------------ ----- ~~~~-T--n--r----------_ WfsUOC1CYJA 7 +±. n *3D~0LqujrbI1Jp 1 + 4L . ODO0DI{LIQOAJDt-* ' a~JO//sOqS)Wfv --- -- -- - G0oo OLL C J - ,- Xko I - ------------- .'- --- ----,3------------------ ,1 1E I I-n ' 1 + ! ! /i Q ] +i - f t, ; S~TtCi GQJ ) ,'{*] i , i,+ ^ . Ds -:. Di~~~~~~~~I * 1 1 1 i+1J Uf;_pUGp to )OU,01- Li t, : I+ ;-f ---- --- --- --- --- --- -- --' - - --- ----- sb6aVI- : l 4 -t), /f~ ]'+ + I t , e4 *riu , rl - g rl F ri n Ji J;g t) lJ -;----- w------ ----r ------------------ ---- _----- .qDQN iOGS 41' + + + 4- HL ',1r ctl , !2 cJv; i . 1 , C CC' 9-1)(1t 4,)Els O,,r g i n 1 --- ----- ild0t1 .......... "pauzsa 1 1 o , Uaiad sqndi.4 i I- q* ;6.o z olf ?XA A.M. Korotky et a!.: Vegetation history of Kunashir Island, Kurile Islands. northwestern Pacific 321 freshwater benthic A2Io-_ 60 * . | + , _ _ t*4 i 0'-40 - ,,. .-- ----.---- ----- --- - f --- - - -- -- -- ---- - - - - --------t==- _4 . -541(h+40 P ------- S7'5 0I 00 .L ....t, ........... P M ~ ~ ~ ~ i 4 ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~~ ~---- - --------- ---- --- -- ----- -------4- 6T440.0I I 00 - ----------- L . it-- o 40% Figure 8 Percentage diatom diagram for 5-6 ni tacustrine terrace in low current of Lesnaya River, site 5936. rare freshwater diatoms. Cool-temniperate broadleaf forests again prevailed on the island (QuItercus up to 34.8%, U/murs up to 5.3%, Jug/aris up to 3.2%, Carpinus 0.4%, Fagus 0.4%). The polle-n assemblage records warner climate than presenit. dated at 4970 ± 80 BP. Fedyashin Cape On the Sea of Okhotsk side a middle-HIolocene peat bog site 5871 (6395) wvas insvestigated on tle south of the island near Fedyashitn Cape (Figure 1). T'he base of the outcrop (3.15 3.8 in) exposes blue-ey poo-rly sorted sand and black peaty silt with water-plant remains and two ash layers. The "C date obtained fromr peaty silt (6395) is 7910 a 140 BP. The lower ash layer of dacite is corre- lated. with the Golovnin Volcano eruption (Razjigaeva vt a., 1998). The upper rhyolitic ash layer is co-related with Ma-f ash of Mashu Volcano. Hokkaido Isla-Ld. erupted about 7200-6300 BP (Arai et al.. 1986). Spores and pollen in peaty silt are rare. Interbedded dark brown peat and peaty sandy silt with wood in interval 2.35-3.15 in has a pollen assemblage (Figure 10) characterized by high conterat of spores (up to 48%) in a. back- ground of ,arboreal polle:n (up to 68%). Predominance of Quercur (up to 55%) and other broad-leaved genera (Jug/ans, Ulmus, Corv/lus and Phe/lodendron) reflects the developiment of broadleaf ibrests. Alder and willow groves were developed within the lagoon coast and in tiver-e mnouths. Birch and coniferous forests occupied upper elevations. The peat was Conned during the mid- Holocene (14 dates 5900 a 40 BP, 5360 ± 70 BP and 5000 ± 70 BP). The overlyIng sandy peat with the same pollen assernblage indicates regression and wind action. Izmena Bay On the lzmena Bay coast the middle-Holocene deposits were investigated in detail near Khleb-nikov Stream mouth (2 in marine terrace, site 5858) (Figure 11). The base of the site (155-1.85 m) exposes green-grev silty sand with; gravel and well-rounded pebbles and remains of water plants. Two diatom assemblages are identified. The first assemblage (1.7-A1.85 m) consists of mainly marinlie species with prevalence of north-boreal Cocconeis scute/- freshwater planktonic a sspecies (j :JPnV .2 ¼.~~~~~~~~~~~~~~~~~~~~~~~~~~ 2Ct 443 (~~~~~~~~~~~~~ti Ca y.a o 5 3 0) { N p C. 0 *o s; .7= lum (up to 7%), Parala asu/rta (up to 207), Navicula giacialis (up to 5%) and Plagiogvramma stauzr-ophorwn (up to 4%) (Figure I I). Among warmwater species south-boreal Arachnoidi.scus eh/renbergii (up to 2%), Au/iScus act/prts (up to 6%) and hvre//a ctypwolyra (up to 60/0) are foLnd. Presence of freshwater Opeplhora inartyi (up to 11%), Aulacoseira granu/ata (up to 13M), A. itaica (tip to 8%) and Diploneis ova/is (up to 8%) indicates river influ- ence. The assemblage reflects a shallow semi-openI brackish inlet environment and moderately warmi climate. Rare diatoms of vari- ous habitats (1.55-1.7 m) indicate the beginning of cooling and regression. The pollen assemblage (Figu-re 12) consists of arboreat pollen (up to 48.6%), nonarboreal pollen (tip to 8.3%) and spores (up to 43.1%). The dominance of Quteusc (up to 54.3%) and the high content of birch pollen (Bert/a sect. A/bae utp to 12.8%, BI. sect. Coszatae uip ;to 1%, Beaul/ sp. up to 3.3%). anid coniferoLLs taxa (Picea sect. Eupicea up to 8.0/ %, P. sect. O.morica up to 1%, Pinis s/g Haploxylon up to 8.1 %, Alies up to 0.6%) reflect the develop- mnent of oak forests on the lzmena Bay coast, and birch and coniferous forests on Golovnin Volcano slopes. Am. ong spores Polypodiaceae prevail (up to 93%). The climate was warmer than present, for conten.t of broad-leaved pollen in the moderm pollen assemblage is lower (33%). The '4C date of 4600 ± 70 BP obtained from the peat dates the -.marine unit. The sea level had a tlower position than at the maximu--m transgression. The narine unit (1.55-1.85 in) is covered by sandy peat (1,25- 1.55 in). Diatoms are missing in the peat base. The uLpper part of the peat (1.25---1.45 m) includes a rich freshwater diatom assem- blage. Planktonic Aulacoseira granulata (up to 36%), A. ta/ica (up to 30%u) and Tatel/aria /aeastrata (up to 6%) dominate. Among epiphytes and benthic species Diplowics oahlis (up to 8%<>), Eunotia pectinairs var. undu/ata (up to 277%), E. gracdi/is (up to 29%,), Pinnularia brevicostata (tip to 7%), P. virid/is (up to 5%) and P, gibba (tsp to 6%) are abundant. Marine -and brackish dia- toms are absent. A freshwater lake existed in place of the inlet during the regression. The coastline was probably at a sufficient distance frtom the lake so that seawater was not influenced. The pollen assemblage with a dominance of arboreal pollen (up lunu YrqdS __n_ i _j! 'lavp' tiunpodow)i j v F1,+il+ + lu! npufl .soj "Plfl7' j . jlu/O j! i,,+ - ,i + ei+ +-4_ Li (, I '- ; 4 8p"21 L 27-1O i 1 .., .mixviouzuu) .31rlqoul*ttn ava.)VUOt.M ZflSW'b ~7VdUIWd snu Sni ds pvr dLu1N ics vjn 1W451j50 'i.)S ojI ,7vqlV aD;)s vin uojfixojdvH i- S $s voldtoln7 P1:75 VD sq PU 1 uz>llo~d p up So W ^___ . tFL .jLLLiiJ~- d . +7- p- + * -+ +-t 4- + + iun1 + f"{]] , 'i4+ _~~~~~ ++ + '. + +,, i.t t- . -------------r------~----- -- ------ ----~~-----~- 4 tl9 J --- - ---- - --------- _-_-_-- -I~~~~~~~~~4 * 18 >><21+ , + i + -H !, t - a 0 ¢Ux9+~~~~ ~~~~~ + + Rtlt fl R n.9 m '1lu~ J | lEJn *1rT .[T n + r 1 -T i5 9Jv . : , d- -F4-t- -tl~~~~~~~~~. a . . .4 ; 1.: n . h n jP xq - il- in ' n5nlaXn drS . ', 11; + ,. ,,li~~~~~~~~~l: i 'tC1 &w~~~~~~~~+ L + . E itLltj!28 121|V l , ~~~~j,5 322 The Holocene 10 (2000) ultniv , C. es ._ v ; , - *,, ., J . ,_ - - ;) C . _ , as .. ._ - - CX - :' s.. . V . C5 - F.i. C} ,v , & *_1 0 1. 'I I I A.M. Korotky et a!.. Vegetation history of Kunashir Island, Kurile Islands. northwestern Pacific 323 o ,r ;Rz~ssodeuo 1 - W - rt 4-'- il + aOueL!WDJ9 .+.j , ++v Xl . **l* l * *k Jp sral~o//t + snjAio'jJ supfbnp + sr) ~ nY + F- I I snoienO snui V Je'S/Dui.Jv 4 dOP ! D iflI9 ------------- ----------- e osqni9 : 0- - n PtzUJDylo .e~ fi | ++ -t -0- ++ + r~j61 slqV. rl. F',p' +' ,0 CD, VAII@ - - -- . --- --- M-*------- 0 ~~~~~~~- A iollod ~ d d dn ci!;s Q ~ ~ ~ ~~ ~ ~~ ~ ~~~~~~ ---------- pur)( lse, ---at ----- 324 The Holocene 10 (2000) freshwater planktonic _________r_ arine and blrt ki ,h species ..E spec~es c CO jO .] Z t3 to- 3 CS ~> toO 0QoomC Lz-Qb 0 qt0~O C - freshwater benthic species o t O, E j S 5Cg E I o'D. >,_q~~~~q~~r__-_w_ > ,~~~L. _L- _Z i__C~ C.I < < ~< iLL . Z fI: 1_ 12C.L -Z ---- ------E 1 L -L- ---------- I J A . ~ ~~~~ q. 1 167 %itt + ~~~~~~~~~~~~~~~~~~~~~~~- F,----.n,* ----' t--: - - - --- B-- >t - --- .~~~~~~~~~~~~~~~~~~~~~~~~~- - - - - Er --------------- t ........--- -- ------ -- I..4-;--- - - - - - ~ ~ ~ ~ ~ ~ ~~~~~~~~~~~~~6 6 .. . . . . . . i Stt. ... ...,... ... .. ...... .... ... X. ... ... .. . . . . . . . . . . . . . . . . T . . . .. +, . 5> t t . .g e t, r. t. t s . ......................................................... ............... ..... .-~*-~ 1 - i- 1 4 3-_ --- --- - --- --- --- - --- - --- --- -- --- --- - 2 Figure 11 Percentage diatom diagram for 2 m marine terrace near Khlebnikov Stream mouth, site 5858. to 90%) indicates the wide development of oak forests (Quercus up to 82%,S,). Coniferous and birch pollen increase. Hligher contents of A/naster and ildyrira reflect wetland formation. Herb pollen and spores are less diverse than in the marine deposits. The '4C date is 4600 ± 70 BP. Late-Holocene deposits Kosmodernyanskaya Inlet The terrace in-cludes the series of storm ridges (Figure 2) dated 2020 :L 90 BP on shelfs at site 5708. The diatom assemblage froim the green-grey beach sand of site 5815 (0.65-1.70 in) includes Futor/a pracrupta (up to 44%), Pinnilaria b orealis (uIp to 11%"() and! Hantzschia ar-uphxiYryvs (up to 6%), whichn indicate swamp (Davidova, 1985) (Figure 3). Ter pollen assemblage reflects development of co:niferous forests (Ab/e ulp to 54.5%,/,, Picea sect. Eu/iceo up to 2.6%, P. sect. Omorica up to 18.2%) with birch alnd alder (Figure 4). The content of broad-leaved genera is sharply decreased at the top, demonstrating climatic cooling. Deposits from the top of the tenrace 5815 (Figure 2) are represented by brow-n-grey aecolian sand with two ash layers (Korotky et al., 1995), correlated with ash Ma and Mb of Mashu Volcano, dating about 0.6 ka (Arai et al. 1986). Serebryanka River Late-Holocene marine deposits were found within peatland of South Kurile Isth-mus (site 5822) (Figure 5). Green-grey saind with rare boulders (1-4- 1.9 m) includes a matrine diatom assemblage (FigLtEe 6). North-borenl Pa/afia sulcata (Up to 82 ¼jO) anLd south- horeal sublittoral Aecitiocyclus octonarius (up to 85%) dominte. Species typical for semi-open shallow inlets, such as Coceoneis scutellum, Ilyalodiscus scotiIcuy, Thalossiosira bramapuntae, )dontel/la aurita, Campy/od/scas daemel/anus and Delphineis sur/rel/a are found. The pollen assemblage with predominance of broad-leaved genera (Qterctu up to 43%'o. Umay up to 5%z;, JAg- lans up to 5%, PFroxs/nz;, Carpinus, Cory/us, Phellodendron) reflects the development of cool-temperate broadleaf forests and a climate warmer than present. The sand is covered by dark brown. peat and penty silts (1.2-- 1.4 m) vitl similar diatom assemblages. A peak of colder-water Pat-a/ia sulcata is observed in the middle of the unit. Freshwater species such as Diploneiv ovalis (up to 47°%), Fragi/aria con- slrruens (up to 4%), P/nura/ia i'ridis (up to 11%) and Eanotia peci/na/is (uip to 80/a) reflect river input. The pollen assemblage is similar to that of underlying maine sand and is dated as 2780 ± 60l BP. Above this is peaty silt with ash (0.85-1.2 ni) containing marine and freshwater diatoms (Figure 6). High content of marine warm- water Actinocycluv octonarius aind freshwater Di/loneis ovalis are found. The pollen assemblage is characterized by low contents of broad-leaved taxa. Conifers (Picea sect. Eupi/ce, P. sect. Omnor- ica, Abies) dominate. reflecting the development of boreal conifer- ous forests. Prevalence of pollen of small-leaved taxa at the top (Retw/a sect. A/hoe up to 46%"40. B. sect. Costoate up to 14%,''0 Bet-aa sp. up to 22%) indicates cooling ('IC date 1960 ± 80 BP). An ash layer is correlated with ash Ma-d of Mashu Volcano. Iokkaido, erupted nabout 1.7- 1.8 ka (A.rni et ao, 1986). The uppermost peat unit is represented by interbedded black peat and light brown. peaty silt with ash (0.3--.85 m). Freshwater benohic Pinnularia v/ridis (up to 3)O%) and P. .s.a-Wapuaro (ulp to 22%) and epiphytes Eunotia peectnaois (up to 13%), E. valida (up to 70%i) and.E. tenclla (up to 9%i,) dominate in the diatom assem- blage. The pollen assemblage rellects the development of boreal coniferous forest on the coast at '4C) date 600 ± 60 BP. Thle ash layer is correlated with Ma-b of caldera-forming eruption of the MashU V'olcano, Hokkaido, dated 6'0 ± 110 BP (GaK-1 1374) (Arai et a/.. 1986; Sakaguchi et a/., 1985). The top of the section exposes a. sand unit1. (0-0.3 in). The pollen assemblage with prevalence of pollen of broad-leaved taxa. The diatomo assemblage includes a high content of the marine Para/ia sacaota (up to 87%) and ActinocyciUs ocronarius (up to 50%). Pollen anid diattom assemblages are similar to those front the mar- ine unit exposed in the lower part of the site. The sand unit was redeposited by humans. Lesnaya River The lacustrine environnent was also studied ir. a 5-6 m terrace section of Lesnaya River (site 5936) (Figure 5). Thie deposits are represented by thin interbeddedl light brown clay and peaft (1.3- 1.65 mi). The dominance of Quercus (up to 52. 1%) and low diver- sity of other broad-leaved genera (Figure 9) reflects thie develop- ment of oak forests on the coasts. Climate was warmer than present, because conlifers are the most abundant in Lesnava River valley now. The deposit is dated 4260 - 60 BP. Deposits from site 5936 include at the top green.-grey clay (I-- 1.3 us) with ash layer (1.2-1.24 m) and two soil horizons with ash 6858 °rrrrl -. - - s--T r, i -] .E. a 1. ' 2070+30 Pt 27304;60 D 3 790 4- 7T0 0 4 600t -70T A.M. Korotky et a!.: Vegetation history of Kunashir Island, Kurile Islands. northwestern Pacific 325 S 36;qJC iW sSV U) Co CJ __ __ __ __ __ __ __ ._ __ __ __ __ ._ __ __ 0_ _. __ uwnubioudS (kinJiDL/do LAfJ0Oo/0 I~frqpodioAv7 opunuwsO XK)O!PG(1AOdd aeoeD~iOGOsu(8 eooooln~~vounud EcE3:c00i13 DE)ODffQSfilU eopsoduot-no EDJGUIWADJS eoe0oedAQ UOJPUiPOgta'4d snudio j snuflD .Si JUflQ JeSJfUIV *ds olnno or-J0so$) 4DOs DfjnlEL, (,O*P/'Ic Nos F9r1ud u oI/XoUdsH 3/S .SO-U~d D"OO/f(l3 4+)OS DG-)d OIJowO 'Joes DAJ/d-; Se-/cpv saJodS ClIGH ojellod sqn1its PLUD SEO)E * . - L.~~~~~~ +~ Uflu. 4L -4 + .A -44 - - - ------ I - + (n 4n +j-+ K n a I +-r l,'~ + i 7 - + +..7 : + -; ~~~+ + n :1+ _1 a r+ +i . r + ......... f lvi4++'4- - t --- CD-q ;- __ _ _ _ __ _ _ _ 4 _t* _ * _ _ _ _ _ _ _ _ +0 + D t~ie A _ , _ _ _ _ . ._ _.. . ._ r C-_ CN-+i --fn--1q84 a co ~ 7 (wj) Lilder. C6 cjl 0 0cls CN v O'~ C:J - f. 326 The Holocene 10 (2000) layer {0--0.7 nli). The pollen assemblage from the clay unit consists maintly of pollen of smiall-leaved trees (A4nester up to 34.6%, Bernla sect. Nanae up to 200%10, Beun/a sp. up to 11%), which reflects development of birch forests with Alnester and shrub birch. This assemblage shows sharp cooling, high hatuidity and intensive fgus. In the Kurile Islands shrub birch and aider are aburdant on swamp coasts with intensive winds and fogs. Clays are covered with loam and sandy loam (0 -1 ni) with scoria of Mendeleev Volcano. indicating high intensity of slope processes duringr cooling. The pollen assemniblage from the soil is mainly composed of Ahies (up to 43.7%) with other conifers (Picea sect. Eupicea uLp to 3%, P. sect. 0lmoreca up to 4%), small-leaved gen- era (Betrna sect. Casratae up to 9%, B. sect. A/bee up to 14%), and rare broad-leaved taxa (Figure 9). Climate and landscape is similar to present. The ash layer is correlated with ash Ma-b of Masbu Volcano ( Arai et al., 1986). Fedyashin Cape On the southern part of the island peat was found near Fedyashin Cape (site 5871). The pollen assemblage from dark-brown sandy peat unit (1.3-2.35 m) consists mainly of spores (88.4--99%) of Polypodiaceae and Osmunda. '4C dates are 4100 ± 50 BP and 3960 ± 50 BP. The domin-an-ce of spores may reflect a large fire connected with ertuption of Mendeleev Volcano, dated about 4220 ± 50 BP (Lebedev et aL, 1980). The overlying unift is cotnposed of black peaty silt withl scoria and ash layers. Spores prevail at the basis of the unit (tip to 54.9%/a), arboreal pollen at the top (up to 44.7%) (Figure 10). High herb pollen content (up to 38.3%) reflects development of grass- land. 'ree-pollen composition indicates changes of island veg- etation: the conlitents of broad-leaved taxa (Querc-Us up to 9.7%, Juglans up to 1.2%, U/tolns Up to 5.1%. (D ory/us uip to 0.4%, Phel- lodendre? tip to 1.4%) sharply decrease. Abies (u:p to 41%) domi- nates among conifers. and A/tins (up to 74.7%) among small- leaved taxa. The pollen assetmblage -reflects the development of coniferous and birch forests on Giolovnin. Volcano slopes and alder and oak growths on marine coasts. The climate was sinmilar to the pres ent. The ash layer is correlated with a sh Ma-d of Mashu Volcano (Arai et at. 1986). Tne scoria layer probably was formed as a result of a small explosion within Golovnin Volcano caldera. The top of the section. exposes green-grey fine aeolhan sand, with ash layer correlated with ashl Ma-b of Mashu Volcano (Arai et al., 1996). The aeolian cover probably was formed daring the 'Little Ice Age' (Korotky el at, 1996). Izmena Bay On lzmena Bay coast (site 5858) blue-grey and green-yellow silty sand (0.75-1.25 rn) has abundant water plants and rare pumice. The deposits include tvo diatom assemblages. The first asserm- blage (0.971-1.25 m) is characterized by marine species and simi- lar to middIle-IHolocene assemblage (Figure 11), (ominted by sublhittoral north-boreal (T'Cconeiys crtee//lum (tup to 1.3%). Pare/ia sn/cata (up to 12%), Odontella annrita (up to 8%) and Grammato- phora oceanica (up to S8%), and by neritic arcto-boreal species Thalass-iosira naiordens/ioeldii (tip to 8%). Th. gravida (up to 2%), Th. /eptopns (u|p to 3%), Porosira glacialvs (up to 5%) and Rhab- donerna arcnaturn (up to 5%). Marine warn-iwater species are rep- resented by N/icu/a granulate (up to 1S%), Tha/as.sionema nitz- sc/i/oide.s (up to 4%) and Acdinoptychus senart -ins (up to 2%). Freshwater species include .A/tacoseira ital/ca, A. granulata and Dip/io.ns ova/is. The diatom assemblage reflects open inlet with river input. The top of the Unit includes rare marine and freslh- water diatomis. The second diatom assemblage (0.8-0.85 m) conitains mainly freshwater Fragilaria pinnata (up to 67%). Dip/one/s ellipitica (up to 4%). Rho/baiodia, museuids (up to 7%,n) and Fyi/temia z7ebra. Marine species such as Nitzscha granulata (up to 7%), A/i&SCUS sculpinis (up to 2%), Para/ica sicatca (up to 2%n) and Nevicula granulata (uip to 2%) are typical for a strongly brackish shallow marine inlet (Jouse, 1962). The sea level was slightly higher than present. Arboreal pollen- (44.8%) and spores (41.9%) dominate at the base of the m.arine unit; arboreal pollen dominates at the top (up to 82%,). Nonarboreal pollen ranges from 5.9 to 13.3%. Broad- leaved taxa represented are mainly Quercus (up to 78.5%) in association with Jiglans, U/inus, Coiy/us, Carpinu.r and Fagwv. The pollen assembltage reflects development of cool-temperate broadleaf forests and a warner climate than present. Thle '4C date from the overlying peat unit is 3790 ± 70 BP. The sand is covered by peat and peaty silt (0.35-0.75 t) with poorly sorted sand layers and ash. T[>he ash is represented by rhyo- lithic light-yellow silt (SiO2 of 70.35%). The pollen .assemblage includes a high content of spores. Amorng arboreal pollen Querens dominates (up to 65.5%,,), which reflects the development of oak forests on the coast+. Diversity of other broad-leaved genera decreases. Eticaceae pollen is abundant. High spore content occur (up to 61.1%). Among spores Polypodiaceae prevails. The '4C date of 2730 ± 60 BP is from the middle of the peat unit. Sharp maxima of small-leaved taxa pollen (letu/a sect. Costarte Lip to 18%/0, B. sect. A/hoe tip to 23.5%, A/,lnos up to 18%) occur near the top of the peat where Querens pollen decreases to 19%. Such a pollen, assemblage reflects climniatic cooling, with dates as 2080 ± 80 BP andid 2070 ± 30 BP. An ash layer is correlated with ash F.niwa I of Eniwa Volcano, Hokkaido Island, which erupted about 2060 ± 100 BP (Gak-3740) (Taira. 1980c). The top of site 5858 is composed of dark brown sandy loam (0.15-0.35 m) wit. ash layer and soil (0-0.15 m) (Figure 12). Arboreal pollen decreases (up to 48.7%), and small-leaved genera dominate (Bernla sect. Cosarrte tip to 16%, B. sect. A/hae up to 33%, A/nuts up tol'3%), with rare Beurna sect. Nnae nand A/n asrer. Broad-leaved taxa are mainly represenited by Quereuns (up to 26%). The high contents (up to 23%) alnd large diversity of herb pollen and the presence of JW/yrica (up to 27%) reflect develop- ment of grassland and swamp. Climate was similar to the present. A soil profile formed on aeolian sand. The ash layer is correlated with ash Ma-b of caldera-forming eruption of Masha Volcano (Arai et at, 1986), so the soil was formed about 500-600 BP. Discussion Kunashir Island was a peni-sula of Hokkaido Island before the Ilolocene began. Vegetation development and environmental evolution of these areas have many comnmon featuresl Table 3 shows major Holocene eveents on Kumashir and their correlation with the Japanese Islands. Changes of natural processes in tlhis region were controlled both by global climatic changes and by such regional factors as migration of warm and cold marine cur- renits. On Hokkaido dtry and cool climate changed to watm and moist about 8000 BP, when the Tsushima Current reached die coast of northern Japam against a background of global warning. This palaeogeographical event resulted in a sharp transformation of vegetation. So the forests with Juglans-Bernal and A/tins- Jug/ans in river valleys and Pieea-Ahies on marine terraces and slopes were replaced by cool-temperate broadleaf forests and mixed coniferous-broadleaf forests. a main component of which was Querenas (garashi, 1993; 1994; Tsuknida, 1986; 1988). On Kunashiri lsland birch forests were replaced by cool-temperate broadleaf forests about 7000-6500 BP. This age i-nlterval is marked by ash layers of GiJovnin Volcano and Mla-f of Mashhu VolCao. Maximumrn warming orn Kunashir Island is dated about 6500-- 5000 BP. About 6500 BP Querews expanded across Ktnashiri and became the main co-mponent of the cool-temperate broadleaf A.M. Korotky et a!.: Vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific 327 5 Il v - -t C I - I_ 1 e - .E -5 t-- U7, II .2 .3 ;< VS C) ''.) . _ .o 4-, P0 fV- LZ ,: cl t ) C. VI ._ cl r0) I I 7e I 0 , (45 Cl _: 4-) t -1)E I . ) - , 4* Tl n .o E ---- --- ------ ~s _ _ _ _ _ j - 44~~~k 'a 'i' " S - Ni - I ~ 'a W ~ ~ ~ ~ ~~ ~~~ ~~~~~~~~~~~~~~~~~~~~~W C" I I F_ oo '-4 44 i* _H -_-- _--'--- -'--4 - -. N /~~~~~~~~~4 - ~lCN C ------ ------ - -0ir 4 -, --,) W o _. o 0r 0) 0 C4 --i C 40 -C P C U 0 C 0 0 C '4, C C 44 0 41 14 0 C 0 0 C .4, 'C -4 .4' -'-4 - 9 . -- I T . T I I I I I _ I I i I II II I I I 328 The Holocene 10 (2000) forests occupying much of the island. Other deciduous broadleaf trees included Juglans, Ulmus, -Phellodendron, Cotylus, Fraxinst, Tiita, Fagus. Castanea, Carpinus. Pterocarya, A4raia, Acantho- panax and Syringa. The modern distributions of Fagus and HPero- Ocaryn are limited to the Karamiatsunai Lowland in southern Hokkaido (Igarasli, 1993; Tsukada, 1988). Mixed coniferous- broadleaf fo-rests occupied northern Kunashir. Pollen assemblages of middle-Holocene deposits of Kunnashir Island are correlated with pollen zone R1u of the Japanese islands. distinguished for 7(?000--4000 BP (Tsukada, 1986). This warmi phase is correlated with Earlv 3o0mon warm.ing of the Japanese Islands and the Holo- cene Optimlum of Sakhalin and Primorye (Sakaguchi et at., 1985; Korotky anid Kbudyakov. 1990). A migration of vegetation zones to the north is correlated with global warming (Sakaguclhi. 1983) and the influence of warm currents. We suggest that mid- Holocene vegetation of Kunashir wias simnilar to southern H1bk- kaido modern landscape (Tsukada. 1988) and estimate that imean annual tempe-rature was 3 0C higher than present. The Tsushima current flowing off' Japan at this time (5900-47;00 BP) reached north Hokkaido as far north as 450N' latitude (Taira, 198Oa; 1992; Taira and Lutaenko, 19933). Kuroshio strear ;activity then. is con- finrmed by fossil littoral mollusc assemblages. Along the Okhotsk coast of northern Hokkaido the littoral molluscs, whose modern analogues live at S -6 latitude to the south, were found in the middle-Holocene deposits (Sakaguchi, 1983). In this area the minimum temperat-ure of the surface water at the Climatic Opti- mum was estimated to be about 5°C higher than present and was compared with the water temperature of northern Honshu (Matsushima and Onshima, 1974). The maximniun sea-level rise at Holocene transgression coincided with the climatic optinmun. The elevation of coastal line can be estimated from lagoon deposits with "IC date 6520* I 0 BP. on east coast of the Lagunnoe Lake (site 5801). rhe presence of marine diatoms in lacustrine deposits also indicates high sea level. The elevation of deposits allows us to establish that sea level reached up to ±2.5-i-3 in above PSL. The 4(C date obtained from mollusc shells of 'urhicbla Japonica of the Sarobetsu peat- lands, northern Hoklkaido with elevation -4-2.5 m above P81.. is 6370 ± 1 10 BP (Sakaguchi ea al., 1985), which is consistent with our data. These data are well correlated with maximuLm amplitude of Holocene tr-ansgression of Japanese Islands, Sakhalin aInd Pri- morye (Korotky and Khudyakov, 1990; Kulakov, 1973; Sakagu- chi. 1983; Sakaguchi and Okunmura, 1986). At inid-Holocene time the coastal line of Kunashiri Island was more irregular. Large inlets and shallow straits (up to 25-30 in depth) were developed within low isthmuses (Figure 13). The sea- level rise led to active abrasion, causing a large volume of detuital material to enter the coastal zone. Most barriers and numerous separate coastal lakes were forned then. The barrier separating Soutih Kwuile Inlet and (iolovnin Inlet was dated as 5020 ± 100 BP. The lak-es have passed through hydrologically 'open' and 'closed' stages, caused not so much by climatic changes as by geologic processes in a coastal zoie. The growth of barrier forms at this time may have led to increased depth of the coastal lake (5936). Weak cooling about 5700-5400 BP in Kunashir led to a slight regression and development of alder forests on the coast and within river valleys. Sligiht regression on the Japanese islands occurred about 6100-5900 BP (Taira, 1980a). The ,next cooling is dated about 4700-4500 BP. Pollen assemn- blages show that the island vegetation changed slightly. Possibly this resulted from the effect of wann currents. The diversity of cool-temnperate broadleaf orests decreased, but oak forests were widelv distributed on the south. Decreases of broad-leaved taxa and increases of coniferous taxa occurred in mixed forests con the north. The Holklkaido vegetation at this time did not change much eitheir (Igarashi and Kumianio, 1974; Tsukada. 1986). The most significant regression of sea level in the middle to late HIolocene is connected with thiis cooling, w-hich caused the fionnation of extensive dutnefields on the coast (Korotky et al.. 1996). The sea level is estimated to be 4-5 ni below PSL during this regression (Korotkcy and Khudyakov, 1990). The regression about 4500 HP is correlated with the middle Jonnorn regression by Ota et aci (1982) or Kemigawa regression by Sakaguchi (1983). In the late Ilolocene about 4000 BP the central part of the istand was occupied by mixed coniferous-broadleaf forests with domi- nant Aties among the conifers and with less participation of titer- mophylous broad-leaved taxa in comparison wvith i the Holocene Optinunm forests. Cool-temperate broad-leaved forests were developed in the souti. Mass development of warmwater diatom species Actincyciuls octonariuts (Jouse, 1.962) in coa-sti-al w.aters of Kunashiri Islatd indicates a warnwater environment. Warm cutrents reached north Hokkaido at this time (Tairn, 1992; Taira ad. Lwtaenko, 1993). The warming in -the late-Holocene begin- ning is also recorded in palaeolandscapes of the Japanese Islands (Salkaguchi, 1983; Sakaguchi at al., 1985). Significalt changes in vegetation took place on Kunashitri Island during late IHolocene, for pollen results indicate a climatic deterioration after 3500 HP. The northern boundary of mixed coniferous-broadleaf forests shifted south in the Sernovodsky Isth- mus region, and boreal coniferous forests with dom-ninant Picea occupied a large part of the istand. The cooling about 3500-3000 BP had a strong influence on veget.,ation in the Japanese Islands, for coniferous forests were expanded on Hokkaido Island (Tsukada, 1988). Abier increased and for.-med 'Pan--mixed forests' with Alnus, Qutiercus and Ul/ins about 2000 BP (Igarashi, 1994). Two high sea-level positions about 4010--3400 BP and 2950-- 2620 BP (Korotky eac atL. 1996) are correlated with Late Jomon transgression (Funabashi Transgression) of Japan Island (Sakaguchi. 1983). Elevation of the Units with marine diatoms indicates a transgression with sea-level rise about 1.5-2.5 in above PSL and later 1.2 1-.5 in above PSL. Marine diatoms in lacustrine deposits of the peripheral part of the palaeolakes (site 1 8-93) indi- cate higher sea-level position than, modern during the first warm- ing (Korotky et ai., 1995). The increase of marine diatoms from late-Hiolocene deposits of the sites located in Lake Furen. Nemujro Bav coast, eastern Hokkaido (Ohira ea a.. 1994), also i lndiicate two phases of transgression. The transgression led to erosion of the dunefields and abrasion of the weakly lithified rocks. The sup- ply of terrigenous material in dte coastal zone during these trans- uressions resulted in the rapid progradation of sediments at the coasts and filling of the inlets. The formation of the Veslovskaya Spit on the south began at this time. Some authors suggest that e sea-level rise during the Holocene transgression was maximal tin the beginning of thle late, Holocene. According to Bulg.akov (1996) the peak of the Holocene transgression occurred about 4000 BP, and Holocene tratnsgrtessiotn did not exceed. J n above PSL in the Kurile Islands. The same data apply to for Japanese Island coasts (Furu-awa, 1972; Fujimoto, 1990; 1993). These reconstnictions were made foi widespread fragments of late- Holocene accumulative landforms on the Pacific Island. The mid- Holocene coastal line is preserved only within. the back side of peatlands. and it was strongly eroded during later sea-level oscil- lations. The cooling coinciding with the slight regression was fixed about 1700-1300 HP. This cooling is correlated with the Kofun cold stage of the Japanese Islandis (Sakaguchi, 1983). The begin- ning of this Cooling is recorded by a sharp increase in small- leaved genera aind decreases in Quercus pollen dated 2080 ± 80 HP and 2071) ± 30 BP on southehrn Kunashir, well correlated with the beginning of the Kofun cold stage (Sakaguchi. 1983). At this time on Kutnashiri Island there isthmus area increased, and coastal peatland with small lakes was formed in place of the inlets and lagoons. Peatland deposits include marine diatoms, which poss- iblv indicate tsunami or strong stonns. The dune of a secon-d A. M. Korotky et al.: Vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific 329 6500-5500 1 3P : 5000-4000 BP j E 6 FigureD1 Development of Pacific side of South Kur;Ae Isthmuns since 6500 BP. (1) Active cliff; (2) an cent csl. (35 accuunullative, coast, (4) dums.'s (5) storm ridge; (6) present shorelne, generation were formed at this time (Korotky et at.. 1996). Grass- land and swamp landscapes were widely developed on the island. Rare forest in some places and the high humidity caused acti- vation of slope processes. As a whole, the island vegetation was similar to the modern. Numerous ash falls during the last 2000 years mainly frorm Hookkaido volcanoes (Taira, 1980b: 1980c; Arti et a_., 1986; Razjighaeva et at., 1998) have resulted in devel- opment of thick soil profiles. Warming recorded oln the Japanese Islands about 1000 BP (Nara-Heian-Kamakura warm stage) was slight on Ktunashiri Island, although the te.ndency to warming is confirmed by increases in broad-leaved pollen genera. Mari ne terraces (up to 2.5 m) were formed duiring sea-level rise (up to I tl ,above PSL' (Korotky et al., 1995) corresponding to H1ian Transgression of Japan (Sakaguchi, 1983). The lowering of sea level after the slight transgression-a is fixed by algal peat on 0.6 mr below PSI, on the berich near Vodopadny Cape (site 5891), dated 850 ± 50 BP. The cooling and slight regression of the 'Little Ice Age' was chafrac- terized bv intensive accumulation of aeolian material and input of sand to soil profiles on the coastal area. Aeolian landformns of this age include dunes and covers, on buried soils wiith 4C dates of 290 ± 60 BP and 190 ± 40 BP (Korotky et a!., 1986). Conclusions The Holocene enviromnments of Kunashiri Island reflect climatic chanaes and some sea-level oscillations. The migration of warm and cold currents cactively influenced the landscape development. The Holocene Optimum on Kunashiri Island is dated to 7000--0 '1700 BP. Landscapes were dominated by cool-temperate broad- leaf' forests in the south atd central part and by mixed coniferous- broadleaf forest in the north. Climate was warmer thiat present. The warming was coincident with transgression to highest sea- level position about 2.5-3 m above PSL (6500-6300 BP). Nutner- ous barrier coastal lakes were formed at this timne. Diatomn assem- blages allow us to reconstruct hydrologically 'open' and 'closed' stages of development of coastal lakes, caused not so much by ctimatic changes as by geologic processes in a coastal zo;ne Shal- low' palaeostraits occurred on the low isthmuses. The cooling and sea-level drop at 4700-4500 BP led to development of large dlune- fields of first generation due to supply of sandy material from the nearshore zone. In spite of climatic deterioration the island vegetation changed very little due to the warmi currents. This warming at the beginning of the late Holocene was almost similar to the mid-Iolocene.. Cool-temperate forests with1 Qutercu domi- nance had a wide distribution, but the biodiversity of broad-lea ved general decreased. Vegetationl changes and climatic deterioration took place after 3500 BP. Coniferous and mixed coniferous/ broadleaf forests shifted southward and occupied a large part of the island. Two nminor transgressions are recorded about 4010- 3400 and 2950-2620 BP. Active accumulation took place in the coastal zone in this timee Pronounced coolingg was established about 1700--1300 BP. Cool-temperate broadleaf forests developed only in the south. Sligh11t regressio-n led to formiation of the dunes of a second generation. Isth-muses were increased and coastal wet- lands with lakes were formed. Grassland and swamp landscapes were developed as well at this time. Warming about 1000 BP was not intensive. Active aeolian Accumulation took place during the 'Little Ice Age' cooling and regression. 330 The Holocene 10 (2000) Acknowledgements We would like to thank L.P. Karaulova flb providing some of the pollen analysis. We are grateful to Director of Kurile Reserve Pavrk, E. ('rigonev, antl his colleagues for help in fieldwork. The study was supported by Russian Fond of Fundamental Investi- gation, projects N 95-05-15309 and 97-05-65362. We are grateful to Dr H.E. 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Dienst</source>. <volume>36</volume>, <fpage>95</fpage>–<lpage>110</lpage> .</citation></ref></ref-list></back></article></istex:document></istex:metadataXml><mods version="3.6"><titleInfo lang="en"><title>Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific</title></titleInfo><titleInfo type="alternative" lang="en" contentType="CDATA"><title>Middle-and late-Holocene environments and vegetation history of Kunashir Island, Kurile Islands, northwestern Pacific</title></titleInfo><name type="personal"><namePart type="given">A. M.</namePart><namePart type="family">Korotky</namePart></name><name type="personal"><namePart type="given">N. G.</namePart><namePart type="family">Razjigaeva</namePart><affiliation>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</affiliation></name><name type="personal"><namePart type="given">T. A.</namePart><namePart type="family">Grebennikova</namePart></name><name type="personal"><namePart type="given">L. A.</namePart><namePart type="family">Ganzey</namePart></name><name type="personal"><namePart type="given">L. M.</namePart><namePart type="family">Mokhova</namePart></name><name type="personal"><namePart type="given">V. B.</namePart><namePart type="family">Bazarova</namePart><affiliation>Pacific Institute of Geography, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</affiliation></name><name type="personal"><namePart type="given">L. D.</namePart><namePart type="family">Sulerzhitsky</namePart><affiliation>Geological Institute of Russian Academy of Sciences, Moscow, Russia</affiliation></name><name type="personal"><namePart type="given">K. A.</namePart><namePart type="family">Lutaenko</namePart><affiliation>Institute of Marine Biology, Far East Branch of Russian Academy of Sciences, Vladivostok, Russia</affiliation></name><typeOfResource>text</typeOfResource><genre type="research-article" displayLabel="research-article"></genre><originInfo><publisher>Sage Publications</publisher><place><placeTerm type="text">Sage CA: Thousand Oaks, CA</placeTerm></place><dateIssued encoding="w3cdtf">2000-04</dateIssued><copyrightDate encoding="w3cdtf">2000</copyrightDate></originInfo><language><languageTerm type="code" authority="iso639-2b">eng</languageTerm><languageTerm type="code" authority="rfc3066">en</languageTerm></language><physicalDescription><internetMediaType>text/html</internetMediaType></physicalDescription><abstract lang="en">Natural middle-and late-Holocene environmental development of Kunashiri Island reflects global climatic changes and the migration of warm and cold currents. Dry and cool climate changed to warm and moist about 7000–6500 BP, later than on Hokkaido Island. At this time Kuroshio Current system became more active. On Kunashir Island birch assemblages were replaced by cool-temperate broadleaf forests in the south and mixed coniferous/broadleaf forests in the north. The highest sea-level position reached 2.5–3 m above PSL about 6500–6300 BP. Cooling about 4700–4500 BP island vegetation weakly changed that connected with warm current influence. Major regression at this period led to formation of extensive coastal dunefields. The warming at the beginning of the late Holocene was almost similar to the Holocene Optimum. Two minor transgressions are recorded about 4010–3400 and 2950–2620 BP. Active entrance of detrital material to the coastal zone resulted in growth of accumulative landforms. Vegetation changes and climatic deterioration took place in the second half of the late Holocene. Coniferous and mixed coniferous/broadleaf forests shifted southward and occupied a large part of the island. During cooling at 1700–1300 BP the isthmus area increased, coastal wetlands with lakes and coastal dunes were formed, and grassland and swamp landscapes developed. Late-Holocene warming was not intensive. Active aeolian accumulation took place during the ‘Little Ice Age’ cooling and regression.</abstract><subject><genre>keywords</genre><topic>Island arc</topic><topic>environmental evolution</topic><topic>ancient shoreline</topic><topic>palaeolake</topic><topic>coastal dunes</topic><topic>palaeoclimate</topic><topic>sea-level oscillations</topic><topic>vegetation history</topic><topic>Kurile Islands</topic></subject><relatedItem type="host"><titleInfo><title>The Holocene</title></titleInfo><genre type="journal">journal</genre><identifier type="ISSN">0959-6836</identifier><identifier type="eISSN">1477-0911</identifier><identifier type="PublisherID">HOL</identifier><identifier type="PublisherID-hwp">sphol</identifier><part><date>2000</date><detail type="volume"><caption>vol.</caption><number>10</number></detail><detail type="issue"><caption>no.</caption><number>3</number></detail><extent unit="pages"><start>311</start><end>331</end></extent></part></relatedItem><identifier type="istex">3C861CCCB22E160FECFDE16E55CCF4C8ADD11AB4</identifier><identifier type="DOI">10.1191/095968300667552216</identifier><identifier type="ArticleID">10.1191_095968300667552216</identifier><recordInfo><recordContentSource>SAGE</recordContentSource></recordInfo></mods></metadata><serie></serie></istex></record>Pour manipuler ce document sous Unix (Dilib)
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