Na 1 Nachlass Max Horkheimer, 103 - Korrespondenzen u.a. mit Maria Pattermann und Franz Neumann (p. III 11, 1-335)

1 Drucksache der Rechtsanwaltskanzlei Pacht, Tannenbaum & Ross, 1951; 2 Briefe zwischen der Pädagogischen Hauptstelle der Gewerkschaft Erziehung u. Wissenschaft und Max Horkheimer, 1954; 1 Brief vom Pädagogischen Verlag B. Schulz an Max Horkheimer, 1950; 3 Briefe zwischen dem Professor Erwin Walter Palm und Max Horkheimer, 1957-1958; 2 Briefe zwischen Helena Brans und Max Horkheimer, 1953; 2 Briefe vom Park-Hotel Frankfurt an Max Horkheimer,1957-1958; 1 Brief von Enno Patalas an Max Horkheimer, 1 Brief von Theodor W. Adorno an Enno Patalas, 1956; 2 Briefe zwischen Dieter Pätzold und Max Horkheimer, 1952; 8 Briefe zwischen Maria Pattermann und Max Horkheimer, 1952-1958; 2 Briefe zwischen F. Perrot und Max Horkheimer, 1953; 2 Briefe zwischen der Buchhandlung Werner Peter und Max Horkheimer, 1954; 3 Briefe zwischen Alfred Peters und Max Horkheimer, 1952-1953; 1 Zeugnis von dem Studenten Joachim Peter, 1953; 1 Brief von Max Horkheimer an F.H. Peterson, 1950; Briefwechsel zwischen dem Studenten Klaus Peuker und Max Horkheimer, 1951; 1 Brief des Chefredakteuren Karl Pfannkuch an Max Horkheimer, 1955; 1 Brief von Dr. Karl Pfauter an Max Horkheimer, 1952; Briefwechsel zwischen der Studentin Renate Pflaume und Max Horkheimer, 1952; Briefwechsel zwischen Joseph B. Phillips und Max Horkheimer, 1955; 1 Brief von Professor Josef Pieper an Max Horkheimer , 1951; 1 Brief von Ehrenfried Pihan an Max Horkheimer, 1953; 1 Brief von F. G. Pincus an Theodor W. Adorno, 1954; Briefwechsel zwischen dem Professor Koppel S. Pinson und Max Horkheimer, 1956; 2 Briefe zwischen dem Professor Kurt Pinthus und Max Horkheimer, 1953; 1 Brief an Dr. Knut Pipping von Max Horkheimer, 1950; 2 Briefe zwischen Erwin Piscator und Max Horkheimer, 1954; Briefwechsel zwischen der Max-Planck-Gesellschaft zur Förderung der Wissenschaften und Max Horkheimer, 1953-1955; Briefwechsel zwischen dem Professor Richard Plant und Max Horkheimer, 1953 und 2 Briefe zwischen Professor Richard Plant und Margarete Feretty-Füredi, 1953; Briefwechsel zwischen dem Professor Johann Plenge und Max Horkheimer, 1951-1952; Briefwechsel zwischen Barbara Pleyer und Max Horkheimer, 1954; 1 Brief von Erich Paul Pechmann an Max Horkheimer, 1952; Briefwechsel zwischen Dr. Gerhard Poetzsch und an Max Horkheimer, 1958; Briefwechsel zwischen dem Committee on Science & Freedom und Max Horkheimer, 1955-1956; 1 Brief an den Professor Rudolf Pohl von Max Horkheimer, 1953; 1 Brief von der Zeitschrift "Die politsche Meinung" an Max Horkheimer, 1956; 1 Brief von Max F. Pollack an Max Horkheimer, 1954; 1 Brief von dem Professor Wilhelm Polligkeit an Max Horkheimer, 1951; 1 Brief von dem Poli-Verlag an Max Horkheimer, 1950; Briefwechsel zwischen Alexej Poremsky und Max Horkheimer, 1955; 1 Brief von Rita Post an Max Horkheimer, 1952; 1 Brief von Max Potzin an Max Horkheimer, 1951; Briefwechsel zwischen dem Oberstudienrat Max Preitz und Max Horkheimer, 1955; 1 Brief von dem Professor Wolfgang Preiser an Max Horkheimer, 1952; 1 Gutachten und Beilagen von Dr. Karl A. Preuschen an Max Horkheimer, 1955; Briefwechsel und Beilagen zwischen dem Direktor des The Commonwealth Fund E. K. Wickman und Max Horkheimer, 1955; Briefwechsel zwischen Klaus H. Pringsheim und Max Horkheimer, 1952-1958; 1 Brief von Curt Freiherr von Preuschen an Max Horkheimer, 1953; Briefwechsel zwischen Rüdiger Proske und Max Horkheimer, 1951; Briefwechsel und Beilagen zwischen Dr. Harry Pross und Max Horkheimer, 1954; 1 Brief von dem Professor Franz Neumann an Max Horkheimer, 1954; 1 Brief an G. H. Graber von Max Horkheimer, 1953; Briefwechsel zwischen dem Quaker Service und Max Horkheimer, 1950; Briefwechsel zwischn Günther Quandt und Max Horkheimer, 1953 und 2 Todesanzeigen, 1955; 1 Brief an den Querido-Verlag von Max Horkheimer, 1951; Briefwechsel zwischen Emil Querinjean und Max Horkheimer, 1955; Briefwechsel zwischen John Raatjes und Max Horkheimer, 1956; Briefwechsel zwischen der Zeitschrift the humanist radical und Max Horkheimer, 1957; Briefwechsel zwischen Sitangghu Chatterji und Max Horkheimer, 1957; 1 Brief von der Radio Corporation of America an Max Horkheimer, 1953; 1 Brief und Beilagen vom Radiodiffusion et Télévision Francaises an Max Horkheimer, 1955; Briefwechsel zwischen dem Österreichischer Rundfunk Radio Wien und Max Horkheimer, 1956; 1 Brief von dem Professor Boris Rajewsky an Max Horkheimer, 1953; 1 Brief an Else Rang von Max Horkheimer, 1950; Briefwechsel zwischen Heinz Raspini und Max Horkheimer, 1956; 1 Drucksache zwischen Hanna Becker vom Rath und Max Horkheimer, 1953; 1 Telegramm von dem Professor Roland Rather an Max Horkheimer und 2 Briefe von Max Horkheimer an Roland Rather, 1957; Briefwechsel zwischen dem Professor L. J. Rather und Max Horkheimer, 1955; Briefwechsel zwischen Phillip Roth und Max Horkheimer, 1958; Briefwechsel zwischen Sibnarayan Ray und Max Horkheimer, 1956-1957; Briefwechsel mit Beilagen zwischen dem Rationalisierungs-Kuratorium der Deutschen Wirtschaft und Max Horkheimer, 1954; 1 Aktennotiz von dem Jornalisten Rasten der dänischen Zeitung Politiken, 1953; Briefwechsel zwischen Wolfgang M. Rauch und Max Horkheimer, 1956; 1 Anzeige der Ingeborg Rauter, 1953; 1 Brief von dem Hotel Reber au lac an Max Horkheimer, 1955; Briefwechsel zwischen Alice Reboly und Max Horkheimer, 1955; 3 Briefe an die Regensburger Zeitungen von Max Horkheimer, 1956; 1 Brief an den Professor Klaus Reich von Max Horkheimer, 1950; Briefwechsel zwischen dem Reinhardt, Ernst, Verlag und Max Horkheimer, 1953; 1 Brief von dem Apotheker Hermann Reitberger an Max Horkheimer, 1955; Briefwechsel zwischen Dr. Paul Reiwald und Max Horkheimer, 1950; 1 Brief von dem Journalist Godo Remszhardt an Max Horkheimer, 1954; Briefwechsel zwischen Dr. Irmgard Rexroth-Kern und Max Horkheimer, 1952; Briefwechsel zwischen Hans Rheinbay und Max Horkheimer, 1955; 1 Brief von der Universität Bonn an Max Horkheimer, 1953; 1 Brief an den Rheinischer Merkur von Max Horkheimer, 1951; 1 Brief an die Rheinische Post von Max Horkheimer, 1954; 1 Brief an Hans Richter von Max Horkheimer, 1954; Briefwechsel zwischen Dr. Hermann Riefstahl und Max Horkheimer, 1957; Briefwechsel zwischen dem Professor Svend Riemer und Max Horkheimer, 1957; Briefwechsel zwischen dem Ring-Verlag und Max Horkheimer, 1957; Briefwechsel zwischen Werner Rings und Max Horkheimer, 1954; Briefwechsel zwischen Martha Ritter-Raabe und Max Horkheimer, 1955; Briefwechsel zwischen Otto-Heinz Rocholl und Max Horkheimer, 1954; 1 Brief von Hilde Rodemann an Max Horkheimer, 1952; 1 Brief von Edouard Roditi an Max Horkheimer, 1951 und 1 Brief von Theodor W. Adorno an Edouard Roditi, 1951; Briefwechsel zwischen der Zeitschrift Studenten-Kurier und Max Horkheimer, 1955; 1 Brief von Karl Roeloffs an Max Horkheimer, 1953; Briefwechsel zwischen der Kunsthistorikerin Hanna Rhode und Max Horkheimer, 1950-1951; 1 Brief an Dr. Anna Ronge von Max Horkheimer, 1954; 2 Brief an Kathe Romney von Max Horkheimer, 1952-1955; Briefwechsel zwischen Dr. Paul Rompel und Max Horkheimer, 1952; 1 Brief an den Zahnartz Dr. Ingo Ropper von Max Horkheimer, 1953; Briefwechsel zwischen Ilse Wallis Ross und Max Horkheimer, 1955-1956; 1 Brief von dem Professor Hans W. Rosenhaupt an Max Horkheimer, 1952; 1 Brief von Rosenthal an Max Horkheimer, 1958; Briefwechsel zwischen dem Generalstaatsanwalt und Staatssekretär Erich Rosenthal-Pelldram und Max Horkheimer, 1952-1956; Briefwechsel zwischen Lessing J. Rosenwald und Max Horkheimer, 1950; Briefwechsel zwischen dem Lieutenant Dr. Alan O. Ross und Max Horkheimer, 1955; 4 Briefe und Beilagen von Günther Roth an Max Horkheimer, 1953-1957; Briefwechsel zwischen dem Professor Wolfram Eberhardt und Max Horkheimer, 1955; 1 Brief an den Professor M. A. Stewart von Theodor W. Adorno, 1955; Briefwechsel zwischen dem Professor Rheinhard Bendix und Max Horkheimer, 1955; Briefwechsel zwischen der Studentin Valentine Rothe und Max Horkheimer, 1957; 1 Brief von dem Student Rudolf Rothrock an Max Horkheimer, 1953; 1 Brief von Guy Roustang an Max Horkheimer, ohne Jahr; 1 Brief von Heinz Maria Ledig-Rowohlt an Max Horkheimer, 1950; Briefwechsel zwischen Ellen Roy und Max Horkheimer, 1956; Briefwechsel zwischen dem Professor Paul Royen und Max Horkheimer, 1954; Briefwechsel zwischen dem Staatsminister August Rucker und Max Horkheimer, 1955-1957 1 Brief an den Staatsminister August Rucker von Leopold von Wiese, 1955; 1 Bericht von Walter Rüegg, 1953 und 2 Briefe von Max Horkheimer an den Professor Walter Rüegg, 1955; 3 Briefe an den Professor Alexander Rüstow von Max Horkheimer, 1953-1958; Briefwechsel zwischen Käthe von Ruckteschell und Max Horkheimer, 1951-1954; Briefwechsel zwischen dem Student Gerhard Rudolph und Max Horkheimer, 1954; 1 Brief von der Ruf und Echo, Arbeitsgemeischaft an Max Horkheimer, 1952; 3 Briefe an den Professor Jay Rumney von Max Horkheimer, 1952-1954; Briefwechsel zwischen Clarence R. Rungee und Max Horkheimer, 1951-1952;

Na 1 Nachlass Max Horkheimer, 532 - Korrespondenzen u.a. mit Otto Kirchheimer und Leo Löwenthal (p. VI 11, 287 - 514)

55 Briefe zwischen Otto Kirchheimer, Anne Kirchheimer und Max Horkheimer, 1937 - 1947; 1 Brief von Otto und Anne Kirchheimer an Frederick Pollock, 06.08.1939; 2 Briefe zwischen der Rockfeller Foundation (New York) und Max Horkheimer, März 1941; 1 Brief von dem Oberlaender Trust an Frederick Pollock, 10.02.1941; 1 Brief von Otto Kirchheimer an Frederick Pollock, 06.08.1939; 1 Brief von Max Horkheimer an das American College Bureau (Chicago), 07.10.1940; 1 Brief von Max Horkheimer an das College and Specialist Bureau (Memphis, T.), 23.09.1939; 2 Briefe zwischen Max Horkheimer und dem Social Science Research Council (New York), 17.12.1938; 73 Briefe zwischen Leo Löwenthal und Max Horkheimer 1933 - 1935; 1 Brief von dem Europa Verlag A. G. (Zürich) an Max Horkheimer, 30.11.1935; 1 Brief von Max Horkheimer an das United States Department of Labor (New York), 03.05.1935; 2 Briefe von Hugo Sinzheimer an Max Horkheimer, 11.06.1934; 1 Brief von Leo Löwenthal an Hugo Sinzheimer, 16.07.1934; 2 Briefe zwischen Leo Löwenthal und Fritz Schiff, 1934/1935;

Mineral resources in Lower Brule Indian Reservation

On the Lower Brule Indian Reservation in South Dakota, about 3 million tons of metallic manganese are in low-grade deposits in the DeGrey Member of the Pierre Shale on the reservation. The geology and methods of mining and processing this sub-economic mineral resource have been studied extensively; technologically, extraction of manganese is possible. However, an efficient, economical method to separate manganese-bearing nodules from the shale host rocks has yet to be found. The manganiferous nodules occur in the Oacoma zone of the Sully shale member (De-Grey Member) which is a subdivision of the South Dakota Pierre Shale formation. These nodular deposits have an interesting similarity in stratigraphical position, lithology and manganese content to those of the Porcupine Mountain area in Manitoba.

Geochemistry nd isotopic composition of Indian Ocean sediments

A down-core 231Pa/230Th record has been measured from the southwestern Indian Ocean to reconstruct the history of deep water flow into this basin over the last glacial-interglacial cycle. The (231Paxs/230Thxs)0 ratio throughout the record is nearly constant at approximately 0.055, significantly lower than the production ratio of 0.093, indicating that the proxy is sensitive to changes in circulation and/or sediment flux at this site. The consistent value suggests that there has been no change in the inflow of Antarctic Bottom Water to the Indian Ocean during the last 140 ka, in contrast to the changes in deep circulation thought to occur in other ocean basins. The stability of the (231Paxs/230Thxs)0 value in the record contrasts with an existing sortable silt (SS) record from the same core. The observed equation image variability is attributed to a local geostrophic effect amplifying small changes in circulation. A record of authigenic U from the same core suggests that there was reduced oxygen in bottom waters at the core locality during glacial periods. The consistency of the (231Paxs/230Thxs)0 record implies that this could not have arisen by local changes in productivity, thus suggesting a far-field control: either globally reduced bottom water oxygenation or increased productivity south of the Opal Belt during glacials.

Age and chemical composition of apatites from five DSDP and ODP Sites in the Pacific, Atlantic and Indian Oceans

Since studies on deep-sea cores were carried out in the early 1990s it has been known that ambient temperature may have a marked affect on apatite fission track annealing. Due to sluggish annealing kinetics, this effect cannot be quantified by laboratory annealing experiments. The unknown amount of low-temperature annealing remains one of the main uncertainties for extracting thermal histories from fission track data, particularly for samples which experienced slow cooling in shallow crustal levels. To further elucidate these uncertainties, we studied volcanogenic sediments from five deep-sea drill cores, that were exposed to maximum temperatures between ~10° and 70°C over geological time scales of ~15-120 Ma. Mean track lengths (MTL) and etch pit diameters (Dpar) of all samples were measured, and the chemical composition of each grain analyzed for age and track length measurements was determined by electron microprobe analysis. Thermal histories of the sampled sites were independently reconstructed, based on vitrinite reflectance measurements and/or 1D numerical modelling. These reconstructions were used to test the most widely used annealing models for their ability to predict low-temperature annealing. Our results show that long-term exposure to temperatures below the temperature range of the nominal apatite fission track partial annealing zone results in track shortening ranging between 4 and 11%. Both chlorine content and Dpar values explain the downhole annealing patterns equally well. Low chlorine apatite from one drill core revealed a systematic relation between Si-content and Dpar value. The question whether Si-substitution in apatite has direct and systematic effects on annealing properties however, cannot be addressed by our data. For samples, which remained at temperatures <30°C, and which are low in chlorine, the Laslett et al. [Laslett G., Green P., Duddy I. and Gleadow A. (1987) Thermal annealing of fission tracks in apatite. Chem. Geol. 65, 1-13] annealing model predicts MTL up to 0.6 µm longer than those actually measured, whereas for apatites with intermediate to high chlorine content, which experienced temperatures >30°C, the predictions of the Laslett et al. (1987) model agree with the measured MTL data within error levels. With few exceptions, predictions by the Ketcham et al. [Ketcham R., Donelick R. and Carlson W. (1999) Variability of apatite fission-track annealing kinetics. III: Extrapolation to geological time scales. Am. Mineral. 84/9, 1235-1255] annealing model are consistent with the measured data for samples which remained at temperatures below ~30°C. For samples which experienced maximum temperatures between ~30 and 70°C, and which are rich in chlorine, the Ketcham et al. (1999) model overestimates track annealing.

Geochemistry of Fe-Mn crusts in sediments of the Central Indian Ridge

Layered Fe-Mn crusts from the off-axis region of the first segment of the Central Indian Ridge north of the Rodrigues Triple Junction were studied geochemically and mineralogically. Vernadite (delta-MnO2) is the main mineral oxide phase. 230Thxs and Co concentrations suggest high growth rates of up to 29 mm/Myr and a maximum age of the basal crust layer of 1 Ma. Whereas most of the major and minor elements show concentrations which are typical of hydrogenetic formation, Co, Pb, Ni and Ti concentrations are strikingly lower. Concentrations and distribution of the strictly trivalent rare-earths and yttrium (REY) are typical of hydrogenetic ferromanganese oxide precipitates, but in marked contrast, the crusts are characterized by negative CeSN (shale normalized) anomalies and (Ce/Pr)SN ratios less than unity. Profiles through the crusts reveal only minor variations of the REY distribution and (Ce/Pr)SN ratios range from 0.45 to 0.68 (compared to ratios of up to 2 for typical hydrogenetic crusts from the Central Indian Basin). The apparent bulk partition coefficients between the crusts and seawater suggest that for the strictly trivalent REY the adsorption-desorption equilibrium has been reached. Positive Ce anomalies in the partition coefficient patterns reveal preferential uptake of Ce, but to a lesser extent than in normal hydrogenetic crusts. A new parameter (excess Ce, Cexs) to quantify the degree of decoupling of Ce from REY(III) is established on the basis of partition coefficients. Cexs/Cebulk ratios suggest that the CIR crusts formed by precipitation of Fe-Mn oxides from a hydrothermal plume and that in hydrothermal plumes and normal seawater the enrichment of Ce results from the same oxidative sorption process. The growth rates, calculated with 230Thxs data as well as with the Co formula, are inversely related to Cexs.

Composition of ferromanganese crusts from the Atlantic, Pacific and Indian Oceans

A collection of layered ferromanganese ores (27 samples) from the Atlantic and Pacific oceans was studied. Trace element and PGE contents were determined layer-by-layer (up to 10 microlayers) in 13 of these samples. The trace, rare earth, and platinum group element distributions, including their layer-to-layer variations, were compared in hydrogenic and hydrothermal crusts from different regions. It was found that the main PGE variations (by a factor of 10-50) are related to their layer-to-layer variations within a given ore field. The distributions of PGE and trace elements are strongly heterogeneous, which is related, first, to different contents of the elements in the layers of different age in ferromanganese crusts (FMC) and, second, to the observed regional heterogeneity and influence of hydrothermal fluids. Geochemical data indicate that CFC formation was mainly caused by the hydrochemical precipitation of material from seawater. This process was accompanied by diagenetic phenomena, water-rock interaction, and influence of volcanic and hydrothermal sources.

Assamblages and cluster analysis from DSDP Hole 22-214 of the eastern Indian Ocean

Multivariate analyses of latest Pliocene through Holocene benthic foraminifera from 61 samples from Deep-Sea Drilling Project (DSDP) Site 214, eastem Indian Ocean were carried out. The 46 highest ranked species were used in R-mode factor analysis which has enabled to the identification of three environmentally significant assemblages at Site 214. Assemblage 1 is characterized by Uvigerina hispido-costata, Osangularia culter , Gavelinopsis lobatulus, Cibicides wuellerstorfi and Karreriella baccata as principal species. This assemblage is inferred to reflect high-energy, well-oxygenated and probably low-organic carbon deep-sea environment at Site 214. Assemblage 2 is defined principally by Globocassidulina pacifica and U. proboscidea and is considered to indicate an organic carbon-rich environment which resulted from high surface productivity irrespective of dissolved oxygen content. Assemblage 3 is marked by Oridorsalis umbonatus, Textularia lythostrota, Hoeglundina elegans, Pyrgo murrhina, and Pullenia quinqueloba as principal species. This assemblage is inferred to indicate a low-organic carbon environment with high pore water oxygen concentration leading to better preservation of deep-sea sediments.

Benthic foraminiferal fauna and isotope record in Holocene sediments of the northwest Indian Ocean

Historically, the Holocene has been considered an interval of relatively stable climate. However, recent studies from the northern Arabian Sea (Netherlands Indian Ocean Program 905) suggested high-amplitude climate shifts in the early and middle Holocene based on faunal and benthic isotopic proxy records. We examined benthic foraminiferal faunal and stable isotopic data from Ocean Drilling Program (ODP) Site 723 and total organic carbon data from ODP Site 724, Oman Margin (808 and 593 m water depths, respectively). At Site 723 the mid-Holocene shift in d18O values of infaunal benthic species Uvigerina peregrina (1.4 per mil) is 3 times larger than that of epifaunal benthic species Cibicides kullenbergi recorded at Site NIOP 905 off Somalia. However, none of the five other benthic species we measured at Hole 723A exhibits such a shift in d18O. We speculate that the late Holocene d18O decrease in U. peregrina represents species-specific changes in ecological habitat or food preference in response to changes in surface and deep ocean circulation. While the stable isotopic data do not appear to indicate a middle Holocene climatic shift, our total organic carbon and benthic faunal assemblage data do indicate that the early Holocene deep Arabian Sea was influenced by increased ventilation perhaps by North Atlantic Deep Water and/or Circumpolar Deep Water incursions into the Indian Ocean, leading to remineralization of organic matter and a relatively weak early Holocene oxygen minimum zone in the northwest Arabian Sea in spite of strong summer monsoon circulation.

Response of deep-sea benthic foraminifera to Late Quaternary climate changes, southeast Indian Ocean, offshore Western Australia

The Late Quaternary benthic foraminifera of four deep-sea cores off Western Australia (ODP 122-760A, ODP 122-762B, BMR96GC21 and RC9-150) have been examined for evidence of increased surface productivity to explain the anomalously low sea-surface paleotemperatures inferred by planktic foraminifera for the last and penultimate glaciations. The delta13C trends of Cibicidoides wuellerstorfi, and differences between the delta13C trends of planktics (Globigerinoides sacculifer) and benthics (C. wuellerstorfi) in the four cores indicate that during stage 6 bottom waters were significantly depleted in delta13C, and strong delta13C gradients were established in the water column, while during stage 2 and the Last Glacial Maximum, delta13C trends did not differ greatly from that of the Holocene. Two main assemblages of benthic foraminifera were identified by principal component analyses: one dominated by Uvigerina peregrina, another dominated by U. proboscidea. Abundance of these Uvigerinids, and of taxa preferring an infaunal microhabitat, and of Epistominella exigua and Bulimina aculeata indicate that episodes of high influx of particulate organic matter were established in most sites during glacial episodes, and particularly so during stage 6, while evidence for upwelling during the Last Glacial Maximum is less strong. The Penultimate Glaciation upwellings were established within the areas of low sea-surface paleotemperature indicated by planktic foraminifera. During the Last Interglacial Climax, upwelling appears to have been established in an isolated region offshore from a strengthened Leeuwin Current off North West Cape. Last Glacial Maximum delta13C values of C. wuellerstorfi at waterdepths of less than 2000 m show smaller than global mean glacial-interglacial changes suggesting the development of a deep hydrological front. A similar vertical stratification/bathyal front was also established during the Penultimate Glaciation.

Alkali contents, Sr isotope and U-Th-Pb data for ocean crust vein minerals from DSDP Holes 27-261, 61-462A, and 72-516F

Cation exchange experiments (ammonium acetate and cation resin) on celadonite-smectite vein minerals from three DSDP holes demonstrate selective removal of common Sr relative to Rb and radiogenic Sr. This technique increases the Rb/Sr ratio by factors of 2.3 to 22 without significantly altering the age of the minerals, allowing easier and more precise dating of such vein minerals. The ages determined by this technique (Site 261 - 121.4+/-1.6 m.y.; Site 462A - 105.1+/-2.8 m.y.; Site 516F - 69.9+/-2.4 m.y.) are 34, 54 and 18 m.y. younger, respectively, than the age of crust formation at the site; in the case of site 462A, the young age is clearly related to off-ridge emplacement of a massive sill/flow complex. At the other sites, either the hydrothermal circulation systems persisted longer than for normal crust (10-15 m.y.), or were reactivated by off-ridge igneous activity. Celadonites show U and Pb contents and Pb isotopic compositions little changed from their basalt precursors, while Th contents are significantly lower. Celadonites thus have unusually high alkali/U,Th ratios and low Th/U ratios. If this celadonite alteration signature is significantly imprinted on oceanic crust as a whole, it will lead to very distinctive Pb isotope signatures for any hot spot magmas which contain a component of aged subducted recycled oceanic crust. Initial Sr isotope ratios of ocean crust vein minerals (smectite, celadonite, zeolite, calcite) are intermediate between primary basalt values and contemporary sea water values and indicate formation under seawaterdominated systems with effective water/rock ratios of 20-200.

Geochemistry of basalts of the Indian Ocean

Indian Ocean crust formed at Sites 765 and 766 is geochemically comparable to that presently forming in the Red Sea. In both cases, we interpret the crust as reflecting high degrees of mantle melting that are associated with an enhanced thermal gradient below recently rifted continental lithosphere. Asthenospheric melts formed in this environment are rich in CaO and FeO, poor in Na2O and Al2O3, and characterized by depleted rare earth element (REE) profiles ([La/Sm]n approximately 0.5-0.6). Both the Red Sea basalts and the basalts at Sites 765 and 766 are distinct from those erupted at the present Mid-Indian Ocean Ridge. The isotope characteristics of the Site 765 basalts define a geochemical signature similar to that of the present-day Mid-Indian Ocean Ridge basalts (MIORB). The Indian Ocean mantle domain is distinct from that of the Atlantic and Pacific oceans, and this distinction has persisted since Jurassic time, when the Site 765 oceanic crust was formed.

Maastrichtian calcareous nannofossils of the Indian Ocean and Shatsky Rise

The biotic effects of volcanism have long been the unknown factors in creating biotic stress, and the contribution of the Deccan volcanism to the K-T mass extinction remains largely unknown. Detailed studies of the volcanic-rich sediments of Indian Ocean Ninetyeast Ridge Sites 216 and 217 and Wharton Basin Site 212 reveal that the biotic effects of late Maastrichtian volcanism on planktic foraminifera and calcareous nannofossils are locally as severe as those of the K-T mass extinction. The biotic expressions of these high stress environments are characterized by the Lilliput effect, which includes reduced diversity by eliminating most K-strategy species, and reduction in specimen size (dwarfing), frequently to less than half their normal adult size of both r-strategy and surviving K-strategy species. In planktic foraminifera, the most extreme biotic stress results are nearly monospecific assemblages dominated by the disaster opportunist Guembelitria, similar to the aftermath of the K-T mass extinction. The first stage of improving environmental conditions results in dominance of dwarfed low oxygen tolerant Heterohelix species and the presence of a few small r-strategy species (Hedbergella, Globigerinelloides). Calcareous nannofossil assemblages show similar biotic stress signals with the dominance of Micula decussata, the disaster opportunist, and size reduction in the mean length of subordinate r-strategy species particularly in Arkhangelskiella cymbiformis and Watznaueria barnesiae. These impoverished and dwarfed late Maastrichtian assemblages appear to be the direct consequences of mantle plume volcanism and associated environmental changes, including high nutrient influx leading to eutrophic and mesotrophic waters, low oxygen in the water column and decreased watermass stratification.

Sedimentology and Th, Pa, U, and N isotopic composition of core MD84-527

High-resolution records of opal, carbonate, and terrigenous fluxes have been obtained from a high-sedimentation rate core (MD84-527: 43°50'S; 51°19'E; 3269 m) by normalization to 230Th. This method estimates paleofluxes to the seafloor on a point-by-point basis and distinguishes changes in sediment accumulation due to variations in vertical rain rates from those due to changes in syndepositional sediment redistribution by bottom currents. We also measured sediment delta15N to evaluate the changes in nitrate utilization in the overlying surface waters associated with paleoflux variations. Our results show that opal accumulation rates on the seafloor during the Holocene and stage 3, based on 14C dating, were respectively tenfold and fivefold higher than the vertical rain rates, At this particular location, changes in opal accumulation on the seafloor appear to be mainly controlled by sediment redistribution by bottom currents rather than variations in opal fluxes from the overlying water column. Correction for syndepositional sediment redistribution and the improved time resolution that can be achieved by normalization to 230Th disclose important variations in opal rain rates. We found relatively high but variable opal paleoflux during stage 3, with two maxima centered at 36 and 30 kyr B.P., low opal paleoflux during stage 2 and deglaciation and a pronounced maximum during the early Holocene, We interpret this record as reflecting variations in opal production rates associated with climate-induced latitudinal migration of the southern ocean frontal system. Sediments deposited during periods of high opal paleoflux also have high authigenic U concentrations, suggesting more reducing conditions in the sediment, and high Pa-231/Th-230 ratios, suggesting increased scavenging from the water column. Sediment delta15N is circa 1.5 per mil higher during isotopic stage 2 and deglaciation. The low opal rain rates recorded during that period appear to have been associated with increased nitrate depletion. This suggests that opal paleofluxes do not simply reflect latitudinal migration of the frontal system but also changes in the structure of the upper water column. Increased stratification during isotopic stage 2 and deglaciation could have been produced by a meltwater lid, leading to lower nitrate supply rates to surface waters.