OLR (1982) 29 (12) D. Submarine Geology and Geophysics 773

sequence is older than previously thought (Nelson, 1980, 1981), although not as old as suggested by Feyling-Hanssen's (1980) biostratigraphic correla- tions; the two oldest aminozones may predate the Quaternary. U.S. Bureau of Reclamation, P.O. Box 25007, Denver Federal Center, Denver, Colo. 80225, USA. (dlf)

82:6070 Nelson, C.H., 1982. Late Pleistocene-Holocene trans-

gressive sedimentation in deltaic and non-deltaic areas of the northeastern Bering epicontinentai shelf. Geologie Mijnb., 61(1):5-18.

Seafloor vibracores and high-resolution profiles provide data on the thin, transgressive, sandy non-deltaic facies of the Chirikov Basin and the thick, muddy prodeltaic sequence of Norton Sound. The sediments of this interval are described and compared with similar modern and ancient deposits. USGS, Menlo Park, Calif. 94025, USA. (hbf)

82:6071 Paskoff, Roland and Paul Sanlaville, 1982. Tyr-

rhenian and Wfirmian deposits on western Med- iterranean shorelines. C. r. hebd. S~anc. Acad. Sci., Paris, (II)294(12):737-740. (In French, English abstract.) Dept. de Geographie, Univ. de Tunis, 94, boulevard du 9-avril-1938, Tunis, Tunisia.

82:6072 Thomson, John, 1982. Holocene sedimentation rates

on the Hellenic Outer Ridge: a comparison by 14C and 23°'I'hex~ methods. Sedim. Geol., 32(1/2):99- 110.

C-14 and excess Th-230 techniques yielded equivocal sedimentation data for the most recent eastern Mediterranean sapropel. C-14 values indicate a higher-than-average sedimentation rate while values of excess Th-230 would normally suggest a decreased rate, results indicative of a complex sedimentation process. Inst. of Oceanogr. Sci., Wormley, Godalm- ing, Surrey GU8 5UB, UK. (msg)

82:6073 Thunell, R.C. and D.F. Williams, 1982. Paleocean-

ographic events associated with Termination II in the eastern Mediterranean. Oceanologica Acta, 5(2):229-233.

A sequence of paleoceanographic changes associated with the glacial/interglacial transition at 127,000 yrBP was identified in the eastern Mediterranean based on microfossil and stable isotope studies: rapid increase in surface water temperature, devel- opment of anoxic bottom conditions, and localized

increase in productivity in the region around Crete. These events appear to be a response to the interplay of a global warming with changes in drainage patterns in the circum-Mediterranean. Dept. of Geol., Univ. of South Carolina, Columbia, SC 29208, USA.

82:6074 Wagner, F.J.E. and C.T. Schafer, 1980/81. Upper

Holocene paleoceanography of inner Miramichi Bay [east Canada]. Marit. Sed., 16(1/3):5-10. Bedford Inst. of Oceanogr., Dartmouth, Nova Scotia B2Y 4A2, Canada.

82:6075 Watts, A.B., 1982. Tectonic subsidence, flexure and

global changes of sea level. Nature, Lond., 297(5866):469-474.

Tectonic models for passive margin evolution pre- dict that following rifting, sediments should pro- gressively onlap basement at the margin edge as the lithosphere cools and increases its flexural rigidity. The pattern is strikingly similar to that used by Vail et al. to estimate sea-level rise through geological time; that some stratigraphic sequences at margins may have a tectonic, rather than eustatic, control is suggested by this similarity. Onlap patterns used by Vail et al. may be widespread because several widely separated passive margins rifted at similar times, but they are unlikely to be worldwide. Lamont-Doherty Geol. Observ., Palisades, NY 10964, USA.

D180. Paleontology (see also E-BIOLOGICAL OCEANOGRAPHY)

82:6076 Berger, W.H., M.-C. Bonneau and F.L. Parker, 1982.

Foraminifera on the deep-sea floor: lysodine and dissolution rate. Oceanologica A cta, 5(2):249-258.

Foraminiferal preservation state in a region of the western equatorial Pacific and data on carbonate and J4C sedimentation rates suggest the following: (1) dissolution effects are minor above 3000 m depth; (2) the lysocline is near 3400 m and straddles a marked increase in carbonate dissolution rate (carbonate loss 15 to 20%); (4) only residual assemblages not very sensitive to additional disso- lution occur below 4000 m. A 'linear' model of calcite dissolution with a defined zero loss near 3 km and 100% loss at the CCD provides a reasonably good approximation. The most sensitive preservation indices are fragmentation in the fine sand fraction, and changes in faunal composition of the fraction