Georg Friedrich Händel, Brustbild, anno aetat: 56.

Signatur des Originals: S 36/G01073

Na 1 Nachlass Max Horkheimer, 627 - Unterlagen zu den Vorlesungen "Über den Begriff der Seele seit Leibniz", "Einleitung in die Philosophie" und "Die Aufklärung" (p. VIII 45-VIII 47,1-2)

"Über den Begriff der Seele seit Leibniz" (GS 13, S. 515-569), Vorlesung Sommersemester 1958, Hilmar Tillack: Ausgearbeitete Nachschrift der Vorlesung von Max Horkheimer, Typoskript, 49 Blatt; "Einleitung in die Philosophie", Vorlesung Sommersemester 1959, Max Horkheimer: 1 Heft, eigene Notizen, 8 Blatt, davon 4 leer und 3 zusätzliche Blätter; Hilmar Tillack: Ausgearbeitete Nachschrift der Vorlesung Max Horkheimers, Typoskript 107 Blatt; "Die Aufklärung" (GS 13, S. 570-645), Vorlesung und Proseminar Wintersemester 1959/60, Max Horkheimer: eigenhändige Notizen, 1 Heft, 40 Blatt, davon 23 leer und 21 zusätzliche Blätter (GS 14, S. 146, 145-155); Hilmar Tillack: Ausgearbeitete Nachschrift der Vorlesung Max Horkheimers, Typoskript 70 Blatt;

Ms. lat. oct. 47 - Responsionale secundum usum ecclesiae S. Bartholomaei Francfordensis

Vorbesitzer: Johannes Latomus; Andreas Weber; Georg Gambach; Bernhard Diell

Physical oceanography during Maria S. Merian cruise MSM21/2

Flemish Pass, located at the western subpolar margin, is a passage (sill depth 1200 m) that is constrained by the Grand Banks and the underwater plateau Flemish Cap. In addition to the Deep Western Boundary Current (DWBC) pathway offshore of Flemish Cap, Flemish Pass represents another southward transport pathway for two modes of Labrador Sea Water (LSW), the lightest component of North Atlantic Deep Water carried with the DWBC. This pathway avoids potential stirring regions east of Flemish Cap and deflection into the interior North Atlantic. Ship-based velocity measurements between 2009 and 2013 at 47°N in Flemish Pass and in the DWBC east of Flemish Cap revealed a considerable southward transport of Upper LSW through Flemish Pass (15-27%, -1.0 to -1.5 Sv). About 98% of the denser Deep LSW were carried around Flemish Cap as Flemish Pass is too shallow for considerable transport of Deep LSW. Hydrographic time series from ship-based measurements show a significant warming of 0.3°C/decade and a salinification of 0.03/decade of the Upper LSW in Flemish Pass between 1993 and 2013. Almost identical trends were found for the evolution in the Labrador Sea and in the DWBC east of Flemish Cap. This indicates that the long-term hydrographic variability of Upper LSW in Flemish Pass as well as in the DWBC at 47°N is dominated by changes in the Labrador Sea, which are advected southward. Fifty years of numerical ocean model simulations in Flemish Pass suggest that these trends are part of a multidecadal cycle.

Revista de Filosofía. México, Universidad Iberoamericana, año XVI, Nº 47-48, mayo-diciembre de 1983.

Fil: Yerga de Ysaguirre, M. C.. Universidad Nacional de Cuyo. Facultad de Filosofía y Letras

Nd and Sr isotopic composition of Cretaceous MORB

Chemical and isotopic (Nd and Sr) compositions have been determined for 12 Cretaceous basaltic samples (108 Ma old) from Holes 417D and 418A of Legs 51,52 and 53. We have found that: (1) The chemical compositions are typical of MORB. They do not vary systematically with the stratigraphic positions of the analyzed samples; thus, the chemical evolution is independent of the eruption sequence that occurred at this Cretaceous ridge. (2) REE patterns for all rocks are characterized by a strong LREE depletion with (La/Sm)N = 0.38-0.50; no significant Eu anomalies are found; HREE are nearly flat or slightly depleted towards Yb-Lu and have 12-18 * chondritic abundances. Combining the results of previous studies, it suggests that no significant temporal and spatial variation in magma chemistry (especially for LIL elements) has occurred in the 'normal' ridge segments over the last 150 Ma. (3) lsotopically, 143Nd/144Nd ratios vary from 0.513026 to 0.513154, corresponding to epsilon-Nd(0) = +7.5 to +10, and they fall in the typical range of MORB. However, these rocks have unexpectedly high 87Sr/86Sr ratios (0.70355-0.70470) which are attributed to the result of seawater-rock interaction. (4) The Nd model ages (Tin), ranging from 1.53 to 2.47 (average 2.06) AE, suggest that the upper mantle source(s) underwent a large scale chemical differentiation leading to LREE and other LIL element depletion about 2 AE ago, assuming a simple two-stage model. More realistically, the variation in Tm(Nd) or epsilon-Nd could be derived from mixing of heterogeneous mantle sources that were a consequence of continuous mantle differentiation and continental formation. (5) Because of the low mg values (0.52-0.63), the analyzed basaltic rocks do not represent primary liquids of mantle melting. The variation in La/Sm ratios and TiO2 are not compatible with a model in which all rocks are genetically related by a simple fractional crystallization. Rather, it is proposed that the basaltic rocks might have been derived from some heterogeneous upper mantle source with or without later magmatic mixing, and followed by some shallow-level fraetionations.