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Late-Neogene Paleomagnetic And Planktonic Zonation, Southeast Indian Ocean - Tasman Basin

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Late-Neogene Paleomagnetic And Planktonic Zonation, Southeast Indian Ocean - Tasman Basin

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Content LATE NEOGENE PALEOMAGNETIC AND PLANKTONIC ZONATION f SOUTHEAST INDIAN OCEAN-TASMAN BASIN by Fritz Theyer A Dissertation Presented to the FACULTY OF THE GRADUATE SCHOOL UNIVERSITY OF SOUTHERN CALIFORNIA In Partial Fulfillment of the Requirements for the Degree DOCTOR OF PHILOSOPHY (Geological Sciences) August 1972 INFORMATION TO USERS This dissertation was produced from a microfilm c o p y o f th e original docum ent. While the m ost advanced technological means to p h o to g r a p h and reproduce this document have been used, the quality is heavily d e p e n d e n t upon the quality of the original subm itted. The following explanation of techniques is p ro vid e d t o h elp you understand markings or patterns which may appear on this r e p r o d u c tio n . 1. T h e sign or "target" for pages apparently la c k in g from the docum ent photographed is "Missing Page(s)". If it w a s possible to obtain the missing page(s) or section, they are s p lic e d in t o the film along with adjacent pages. This may have necessitated c u t t in g thru an im ag e and duplicating adjacent pages to insure you c o m p le t e continuity. 2. W hen an image on the film is o b litera ted w i t h a large round black m ark, it is an indication that the p h o to g r a p h e r suspected that the copy may have moved during exposure a n d th u s cause a blurred image. You will find a good image o f th e p a g e in the adjacent fram e. 3. W hen a map, drawing or chart, etc., w a s p a r t o f the material b ein g photographed the photographer fo llo w e d a definite m ethod in "sectioning" the material. It is custom ary t o begin photoing at the upper left hand corner of a large sheet a n d t o c o n tin u e photoing from le ft to right in equal sections w ith a s m a ll overlap. If n ece ssa ry, sectioning is continued again - beginning b e lo w the first row an d continuing on until complete. 4. T h e majority of users indicate that the t e x t u a l content is of g reatest value, however, a somewhat higher q u a li t y reproduction could b e m ade from "photographs" if essential t o t h e understanding of the dissertation. Silver prints of " p h o to g ra p h s " m ay be ordered at additional charge by writing the Order D e p a r tm e n t , giving the catalog num ber, title, author and specific pages y o u w is h reproduced. University M ic ro film s 3 0 0 N orth Zeeb R oad A n n Arbor, Michigan 4 8 1 0 6 A X erox Education C om pany I I 73-779 THEYER, Fritz, 1941- LATE NEOGENE PALECMAGNETIC AND PLANKTONIC ZONATION, SOUTHEAST INDIAN OCEAN-TASMAN BASIN. University of Southern California, Ph.D., 1972 Geology University Microfilms, A XE R O X Company, Ann Arbor, Michigan THIS DISSERTATION HAS BEEN MICROFILMED EXACTLY AS RECEIVED. UNIVERSITY OF SO UTHERN CALIFORNIA TH E GRADUATE 8CH O O L U N IV E R S ITY PARK LOS ANGELES. C A L IF O R N IA 9 0 0 0 7 This dissertation, written by Fritz Theyer under the direction of h.T-.S... Dissertation Com mittee, and approved by a ll its members, has been presented to and accepted by The Graduate School, in partial fulfillm ent of requirements of the degree of D O C T O R O F P H IL O S O P H Y .....................XjDtau , Seotember 1972 PLEASE NOTE: Some pages may have in d is tin c t p r in t. Filmed as received. U n iv e rs ity M icrofilm s, A Xerox Education Company CONTENTS Page ABSTRACT..................................... ix INTRODUCTION ................................. 1 General ................................. 1 Description of the a r e a ................. 4 Materials............................... 16 Lithology of cores................... 16 Methods................................. 19 PALEOMAGNETISM OF CORES ..................... 23 Stability of magnetization ............... 23 Intensity of magnetization ............... 30 Interpretation of magnetic stratigraphy . 33 BIOSTRATIGRAPHY OF CORES ..................... 63 Ranges of selected radiolaria ........... 63 Radlolarlan zones ....................... 95 Ranges of selected foraminifera ........ 102 The Globorotalla truncatullnoides datum plane in the present area . . 120 Planktonic foraminiferal zones .......... 124 Biostratlgraphlc interpretation ........ 127 Core E39-76 127 Core E39-67 129 All other cores..................... 131 11 1 ' I Page Comparison of proposed zones with previous work................................... 134 MIOCENE-PLIOCENE BOUNDARY AND THE MAGNETIC S C A L E ................................... 139 SEDIMENTARY RECORD ........................... 150 Sedimentation rates ..................... 150 Faunal reworking ......................... 153 Gauss-Brunhes disconformlty ............. 155 PALEOCLIMATIC TRENDS ......................... 158 CONCLUSIONS................................. 163 TAXONOMIC NOTES ............................. 168 ACKNOWLEDGMENTS ............................. 171 PLATES........................................ 173 REFERENCES CITED ............................. 187 APPENDICES................................... 199 Appendix I: Numerical paleomagnetic data 200 Appendix II: FORTRAN IV program used to reduce and plot the paleo magnetic d a t a ............. 234 ill ILLUSTRATIONS Figure 1. Index map and location of cores . . . . 2. Generalized physiography of the Australian-New Zealand antarctic sector 3. Cross-section of the Australian- Antarctic Rise along 133° East ........ 4. Major sediment types of the area under study ................................. 3. Generalized bottom currents of the area under study ........................... 6. Comparison of magnetic inclinations in E39-48 before and after partial a.f.- demagnetlzatlon ....................... 7. Comparison of magnetic behavior of isolated samples after consecutive de magnetization under increasing fields 8. Comparison of magnetic intensity with gross lithology and percent sand in selected cores ......................... 9. Inverse correlation between intensity of magnetization and reversals .......... 10. The established paleomagnetlc time scale IIA. Interpretation of the magnetic strati graphy in E39-22 and 24 ............... IIB. Interpretation of the magnetic strati graphy in E39-40, 42, and 44 .......... IIC. Interpretation of the magnetic strati graphy in E39-48 and 50 . . . ........ IID. Interpretation of the magnetic strati graphy in E39-56 ....................... iv Page 2 6 9 11 14 25 27 31 34 36 39 41 43 45 Figure Page HE. Interpretation of the magnetic strati graphy in E39-58 and 6 3 ............... 47 IIF. Interpretation of the magnetic strati graphy in E39-67 ....................... 4-9 IIG. Interpretation of the magnetic strati graphy In E39-76 ....................... 51 12. Generalized correlation of all polarity logs with the magnetic scale.......... 59 13. Ranges of radiolarian and planktonlc foraminiferal indices in the present cores and in previous work............ 69 14A. Blostratigraphic Interpretation of E39-76 ................................. 71 14B. Blostratigraphic interpretation of E39-67 ................................. 73 140. Blostratigraphic interpretation of E39-63 ................................. 75 14D. Blostratigraphic interpretation of E39-58 ................................. 77 14E. Blostratigraphic interpretation of E39-56 ................................. 79 14F. Blostratigraphic interpretation of E39-48 ................................. 81 14G. Blostratigraphic interpretation of E39-40 ................................. 83 14H. Blostratigraphic interpretation of E39-22 ................................. 85 15. Proposed radiolarian and planktonic foraminiferal zoneB and correlation with previous w o r k ......................... 96 v Figure Page 16. Blostratigraphic interpretation and generalized correlation of cores E39-14, 15, 20, 24, 42, 44, 50 and 51 • 132 17. Plots of polarity events against time of selected cores ......................... 151 18. Gllbert-Gauss paleocllmatic trends . . . 159 vi Table Page 1. Locations and descriptive core data . . 17 2. Previous antarctlc-subantarctic radio larian and planktonic foraminiferal zones............................. 64 3. Evolutionary and non-evolutlonary plank- tonlc events in the present material . . 67 4. Radiolarian and planktonlc foraminiferal reference list......................... 88 5. Evolutionary planktonlc events during the Gauss Magnetic Epoch, low to high latitudes............................. vli Plate Page 1. Selected radiolarian Indices ........... 174 2. Selected planktonlc foraminiferal Indices............................... 177 3. Selected planktonlc foraminiferal Indices............................... 180 4. Transitional specimen between Globorotalla tosaensls and G. trunca- tullnoldes .............7 ............ 183 5. Holotypes and paratypes of Globorotalla lnflata trlangula. n. subsp............. 185 vlll r ABSTRACT Paleomagnetic study of twelve predominantly Gil- bert-Gauss deep-sea cores revealed no predictable rela tionship between magnetic stability, magnetic Intensity, and gross sediment composition, although foraminiferal oozes generally showed the greatest dispersion of Inclina tions. Average Inclinations, even after demagnetization, were generally lower than ambient values at the core sites. Intensities of magnetization fluctuated between about 10-5 an(j io"3 emu but values of the order of 10"^ pre dominated. The onset of a reversal usually coincides with a distinct decrease In magnetic Intensity. Adequate paleontological control Is essential to the correct Inter pretation of the magnetic stratigraphy of the present cores. Numerous hiatuses, mixed portions, and short- period polarity events that do not correlate with the established paleomagnetic scale complicated most polarity logs. Analysis of selected radlolarlans and planktonlc foraminlfers In 18 predominantly Gilbert-Gauss cores (which Include the above 12) lead to the proposal of five radiolarian, and four foraminiferal zones that comprise the period t = 0-ca. 5*0 m.y.b.p. These parallel zona- tlons are characterized by partial or concurrent ranges of lx index-species and, In contrast to earlier models, evolu tionary datum planes define their zonal boundaries. Several of these datum planes can also be recognized in the tropics and the North Pacific, consequently facilitat ing world-wide correlations within the framework of the paleomagnetic time scale. Warm-water foraminifers in E39-76 (about 36° S), the northernmost core, allowed the recognition of tropical Neogene Zone 19 and its correlation with middle to late Gauss. Subspecies of the Globorotalla mlozea complex, which the cores share with Mlocene-Pllocene stages of New Zealand, Indicate that the uppermost Tongapurutuan-lowest Kapitean (upper Miocene) correlate with paleomagnetic ages up to earliest Gilbert, the Kapitean Stage with mostly Gilbert-early Gauss, and the Opoitian Stage (lowest Plio cene) with mostly Gauss. The Gauss Epoch w a r a period of biotic transition that can be recognized in all latitudes. Species of Miocene affinities became extinct and Pllocene-Holocene lineages appeared within it. In antarctic-subantarctlc areas the most significant level of faunal change is de fined by the extinction of the G. mlozea lineage among foraminifers, and by the almost coincident extinction of the radiolarians Lvchnocanlum grande. Prunopyle titan, and Stlchocorvs peregrlna. all of which occurred at about 2.5-2.6 m.y.b.p. (late Gauss). _____________________________x_____ Sedimentation rates In the area varied between about 0.3 and 2.0 cm/1000 yr. Estimates of average rates are 0.5 cm/1000 yr for the Gauss and 0.6 cm/1000 yr for the Gilbert. An extensive Gauss age eroslonal discon- formlty Is centered In the area; Its base has an average age of about 2.6 m.y. but some sediments have accumulated locally during the last 0.3 m.y. A systematic outward de crease of the age of the disconformity, as postulated by earlier studies, was not discovered. In addition, the eroslonal feature extends considerably beyond previously defined boundaries, especially west, along the Australian- Antarctic Rise. Five cold cycles occurred in the period comprised by Gilbert to latest Gauss. Of these coolings, two lasted less than 0.1 m.y. and are associated with the latest Gauss and the Kaena event; the remaining three were more severe and somewhat longer. They span, respectively, the Mammoth event and parts of the early Gauss, the middle Gilbert above event "b", and the middle Gilbert below event "b". The coolings were equivalent to northward displacements by at least 10° of latitude of modern surface Isotherms. The warmer lnterstadlals represented conditions comparable to those at the same latitudes today, except for a long and considerably warmer period that terminated just above Gilbert "c" and began below the Epoch 5-Gllbert boundary (5*0 m.y.b.p.). ________________________________xl_________________________________ A new subspecies, Globorotalla lnflata trlaneula. n. subsp., is described which Is apparently restricted to the Gauss Epoch. xil INTRODUCTION General Late Neogene, blostratigraphic zonatlons of antarc tic to subantarctlc areas are based on the pioneering study of radlolarlans by Hays (1965)> and Its subsequent modifi cation and linking with the paleomagnetic time scale (Op- dyke and others, 1966; Hays and Opdyke, 1967; Bandy and others, 1971)* Comparable work with planktonlc foramlnl- fers has been missing. The only regional, foraminiferal zonatlon that Is available (Kennett, 1970) Is related In directly to the paleomagnetic time scale and comprises only the last 1.3 million years (m.y.). This zonatlon did not compare well with the radiolarian ranges In the present material. To Improve this situation, a concurrent analysis of radiolarian, foraminiferal, and magnetic stratigraphy was undertaken In cores from south of Australia and the Tasman Basin. This resulted In a revision of the existing radiolarian zonatlon and the proposal of a new foramlnl- feral zonatlon within the framework of the magnetic time scale (Cox, 1969). The area under study (Fig. 1) contains an extensive dlsconformlty that, except for occasional veneers of 1 Figure 1. Index map and location of cores. Solid circles indicate paleo- magnetically dated cores. Cores were collected during cruise 39 of the U.S.U.S. Eltanln. 2 120* 130* 140* 150* 160' 170* 30* AUSTRALIA MELBOURNE 40* 40* 67 4S 48 015 020 • 6 3 • 44 ,56 058 •4 2 50* 24* • 40 270 60* 150* 160' 170* 4 Holocene in some cores, represents a virtual absence of sediments younger than about 2.6 m.y. (Watkins and Kennett, 1972). Consequently, even the shorter cores penetrated the Gauss and Gilbert Magnetic Epochs (t = 2.4-5.0 m.y.b.p.), and horizons critical for the placement of the Mlooene-Pliocene boundary in deep-sea cores were sampled. In addition, a few tropical planktonlc foramlnifers of the northernmost core allowed indirect correlations with standard Neogene zones of lower latitudes (Banner and Blow, 1965; Blow, 1969)* Moreover, since the cores share faunal Indices with the Tongapurutuan, Kapitean, and Opoitian Stages of the New Zealand Neogene, correlations between the cores and these stages were also possible. This study represents a further step towards generalized planktonlc zonatlon models that ultimately should allow correlations from tropical to temperate and polar regions. Description of the Area Volume 19 of the Antarctic Research Series (Amer. Geophys. Un.), currently in press under the editorship of D. E. Hayes, contains 25 articles devoted to physical oceanography, marine geology, and marine geophysics of the Australian-New Zealand antarctic and subantarctlc sector in which the present study is centered. Papers pertinent to the study are those describing (1) the physiography of the area (Hayes and Oonolly, 1972), (2) structure and sediment thickness as Inferred from seismic profiling (Houtz and Markl, 1972), (3) sedimentary patterns, turbidlte patterns, and manganese pavement production (Conolly and Payne, 1972; Payne and Conolly, 1972a, 1972b; Payne, Conolly and Abbott, 1972), (4) sedimentary dlscon- formltles and Implied changes In bottom water velocities (Watkins and Kennett, 1972), (5) magnetic anomalies and sea-floor spreading (Welssel and Hayes, 1972), (6) nephelold layer and bottom currents (Elttram and others, 1972a, 1972b), and (7) physical oceanography (Gordon, 1972). In view of this detailed coverage, only a descrip tive summary Is presented below. The dominant physiographic feature of the ocean floor between Australia-New Zealand and Antarctica Is the east-west trending Australian-Antarctic Rise (Southeast- Indlan Ridge) (Pig. 2). Welssel and Hayes (1971) trace Its origin to the Eocene (50 m.y.b.p.), when the rifting and spreading of Australia and Antarctica commenced. Over the last 50 m.y. spreading rates varied chronologically and areally. In the eastern sector (along approximately 132° E) rates were about 3.7 cm/yr during the last 5 m.y. (Welssel and Hayes, 1971). This Implies that cores of Gauss age positioned along the northern flank of the ridge drifted about 100 km to the north to their present location and, at the same time, sunk Into deeper waters relative to their original depth. The ridge Is offset Figure 2. Generalized physiography of the Australian-New Zealand antarctic sector. After Hayes and Conolly (1972) and Payne and Conolly (1972b). Closely stippled areas correspond to zones shallower than about 3000 m. Broad stippling indicates extent of manganese pave ment described in Payne and Conolly (1972b). 6 7 50*-I •hclf UTH AUST ABYSSAL A|.J AUSTR SOUTH INDIAN A B Y S S A L ALAI BASIN ■•0"** Risr 60* no* 120* 130* 1 4 0 * 1 5 0 * I—69* 1 6 0 * 1 6 8 * east of 138° E by right-lateral fracture zonee, resulting In a southeasterly trend to about 158° E and 56° S where It Is joined by the Macquarie Rldge-Trench system (Houtz and others, 1971; Hayes and Conolly, 1972; Conolly and Payne, 1972). Between about 120° and 128° E the ridge Is ex tremely fractured, forming the Australian-Antarctic dis cordance. This ridge and other Important features, with bathymetrles, are depicted In Figure 2. A cross-section of the ridge, from Australia to Antarctica along approxi mately 133° E (Fig. 3), shows typical depths encountered In the structurally less complicated zones. Generalized sediment patterns of the area (Fig. 4) are primarily a function of latitude, depth, oceanographic setting, and nearness of the source of terrigenous com ponents. Calcareous oozes (>30 percent CaCOj) are normally restricted to the north of about 50° S and to depths above approximately 4000 m. A case In point Is £39-44 (4132 m) that varies from well preserved oozes (>30 percent sand) to almost completely dissolved foraminiferal debris (<5 percent sand), showing that 4000 m Is a critical depth for carbonate preservation In this region. Siliceous oozes are typical of latitudes south of 50° S. Terrigenous clays Interbedded with siliceous oozes replace these oozes still further south and, finally, thick terrigenous deposits form the abyssal plain off Antarctica (Conolly and Payne, 1972; Payne and Conolly, 1972b). To the north Figure 3 Cross-section of the Australian- Antarctic Rise along 133° E. After Welssel and Hayes (1971). 9 ANTARCTICA AUSTRALIA Figure 4 Major sediment types in the area under study. After Conolly and Payne (1972). 11 I6I*E b r o w n c l a y a Ma n g a n e s e m c4 R E0 US AReo u s ^ / C E O U S of <3600m 40° s r 44° r - 48° h52° h 56° r* 6 0 # 13 of the calcareous oozes (Fig. 4), calcareous clays and silts occur In Intermediate depths (4000-4700 m), and green and brown clays at still greater depths. The south Australian abyssal plain Is a turbldlte deposit containing mixed sandy terrigenous material and foraminiferal- bryozoan debris of various ages and bathymetric origins (Conolly and Payne, 1972; Kahn, 1972). The area east of Tasmania, and the Tasman Basin, again Is characterized by calcareous oozes on topographic highs, calcareous clays In deeper zones, and barren brown clays below about 4700 m. A zone of manganese pavement Is developed south and slight ly east of Tasmania (Payne and Conolly, 1972b). Numerous previous papers discussed the general oceanography of the antarctic area; of these Gordon and Goldberg's (1970) Is one of the latest comprehensive studies. In addition to the aforementioned Investigations, which are specifically concerned with the present region, a discussion of bottom-water behavior by Gordon (1971) Is also relevant. Other sources of Information are bottom photographs and current-meter data published by Jacobs and others (1970). According to their measurements, bottom velocities of up to 15 cm/sec occur In the area south of Tasmania. Condensation of bottom-current data (Fig. 5» after Gordon, 1971) demonstrates the topographic control the area exerts on the generally east flowing Circumpolar Deep Water. Ripple and scour marks, together with exten- Figure 5* Generalized bottom currents In the area of study. Data from Gordon (1971); adapted from Watkins and Kennett (1972). Stippling repre sents areas shallower than approxi mately 3000 m. 14 TASMAN BASIN , EMERALD BASIN SOUTHEAST IFACIFIC \ BASIN 150° 160° 170° 180° 16 Bive manganese pavement south of Tasmania, testify to high bottom-water velocities and consequent erosion (Payne and Conolly, 1972b). Materials Cruise 39 of the U.S.N.S. EltanIn collected 82 piston cores during 1969 In the southeastern Indian Ocean, south of Australia, and In the Tasman Basin. Forty-one of these, and corresponding trigger cores, were processed In the micropaleontology laboratory, University of Southern California. Ultimately, 18 were chosen on the basis of location, length and faunal content. Of these cores, 12 were further selected for paleomagnetic analyses (Table 1; Fig. 1). A few samples of available trigger cores were Included In the blostratlgraphlc and paleomagnetic work (Appendix I) because only they contained the true sediment surface. T.-L. Ku (University of Southern California) 2*30 supplied Th -based dates and D. E. Hayes (Lamont-Doherty Geological Observatory) provided seismic profiling re cords and precision depth-recorder summaries. Lltholoev of Cores Descriptions of gross lithology and colors as well as radiographs of all cores are kept on file at the micro- Table I . Locations and d escrip tive data o f cores Core number Lat. S C ') Long. E (. ,) Depth (m) Dated paleo- Length magneti- (cm) cally Micro fossils Generalized litholoRy Percent sand max. min. E39-14 45 04 125 55 4700 600 fir sil. clay 3 1 E39-15 46 56 126 02 4206 213 f cal. day-ooze 48 14 E39-20 48 01 126 08 4718 952 fir sil. clay 8 1* E39-22 48 51 126 00 4078 355 yes fir cal.-sil. clay 26 1 E39-24 51 08 126 09 4352 1127 yes fir sil. clay 30 1 E39-27 52 59 126 07 4782 992 r sil. clay 20 1 E39-40 52 03 133 57 3255 520 yes fir cal. ooze 73 39 E39-42 49 54 134 01 3328 537 yes fir cal. ooze-clay 57 6 E39-44 47 26 134 02 4132 538 yes fir cal. day-ooze 46 2 E39-46 45 09 133 47 4571 570 fir cal. sil. clay 20 1 E39-48 45 49 136 48 4352 857 yes fir cal.-sil. clay 10 1 E39-50 47 08 142 31 4443 1080 yes fir sil.-cal. clay 15 1 E39-51 47 31 142 00 4718 1113 fir sil.-cal. clay 6 1 E39-56 49 58 145 54 4798 1378 yes fir sil. clay 25 1 E39-58 48 16 147 39 2395 518 yes f cal. ooze-clay 69 13 E39-63 46 58 149 34 3163 514 yes fir cal. ooze-clay 59 18 E39-67 43 38 151 59 2112 1020 yes f cal. ooze 72 33 E39-76 36 30 161 14 3785 992 yes f cal. clay 7 1 f * foraminifera r ■ radiolaria cal. * calcareous sil. ■ siliceous * Contains a turbidite layer in which sandy fraction exceeds 30 percent. 18 paleontology laboratory, University of Southern California. Since the faunal samples taken at 10-cm Intervals were washed through 62-micron screens, a record of the weight- percent of the sandy fraction is also on file. The sandy fraction of the cores is dominated by foraminlfers and radlolarians, and contains only minor amounts of ice- rafted Band and small nodules. Thus, it reflects directly the abundance of the blogenous fraction. Table 1 lists general information for all cores, and Figure 8, which is fully discussed in a later chapter, illustrates the gross llthology of E39-22, 40, 50, 56 and 76. Cores containing two basic sediment types were studied: (1) foramlnlferal oozes, and (2) silty to sandy clays in which calcareous or siliceous sandy components alternate in importance, yet rarely exceed 20 percent in weight. True siliceous oozes, barren clays, and sands were not included. Instead of a detailed description of each core, a summary of representative examples follows. A typioal foramlnlferal ooze, £39-40 (Table 1; see also Fig. 8), contains from 44 to 74 percent sand and, ex cept for minute proportions of radlolarians and ice- rafted quartz, planktonic foraminlfers are the chief components. Colors in it vary from very pale oranges (10 YE 8/2)1 and yellowish browns (10 YR 5/2), to grayish ^eol. Soc. America, Rock Color Chart. 19 orange (10 YR 7/4). Mottling can be seen throughout. Calcareous clays (Table 1; see also Fig. 8) are represented by E39-76, whose sandy fraction generally varies from 0.1 to 10 percent (occasionally more). Carbonate solution directly controls this amount since most sandy particles are fragmented foramlnlferal tests, seldom radlolarians. Colors usually are very pale oranges to light greenish grays (5 G 8/1). Cores with siliceous clays (Table 1), such as E39-56, also contain low percentages of sandy components (see also Fig. 8) but radlolarians dominate over diatoms and foraminlfers. Colors normally vary from very pale oranges to dark yellowish browns (10 YR 4/2). All cores under study contained planktonlc foraminl fers at least at some levels. Most, however, were col lected below solution boundaries and consequently show strong solution effects that limit the countings of as semblages. Three cores contained no workable quantities of radlolarians (Table 1); In many others radlolarians had to be concentrated by solution. Methods On board, while extruding and labeling core sections, the presence of water-gaps, missing sections, and coring-lnduced distortions were noted. This helped later In the core selection. Excess water from the core liners was eliminated on board the ship when possible. 20 Cores with such water were kept vertical and holes were drilled In their liners, which permitted the water to trickle out without disturbing more than the outer sedi ments. Laboratory procedures Involved five steps: 1. Extrusion of the cores In 40-cm segments and splitting these segments In half; 2. generalized description of sediments, Including colors; 3. splitting of one of the halves Into a 1-cm thick slab for radiographing, and an archive section; 4. radiographing; 5. sampling of remaining half at alternate 5-cm Intervals for paleomagnetic and micropaleonto- loglcal studies; paleomagnetic samples were notched to Indicate orientation towards the top. Processing of mlcropaleontologlcal samples followed standard drying, weighing, and screening (62 microns) techniques used by most laboratories. In some foraminiferal-rlch cores It was necessary to dissolve parts of samples with HC1 to concentrate sufficient radlo larians. Counts of foraminlfers are based on fractions^200 microns and on 300 or more specimens. Colling-ratlo counts, however, were done on 100 or more specimens>100 21 microns. Routine analyses of both radlolarians and foraminlfers were made under a standard dissecting micro scope. Taxonomic study of radlolarlan Index-specles re quired the preparation of glass mlcroslldes and the use of a hlgh-power microscope. At the beginning of the paleomagnetic work 2.5-cm- dlameter cylinders, drilled from oriented 5-cm samples, were used. Later, as drilling proved costly In time and broken samples, cubes of about 4 cm^ were punched out of the wet X-ray slabs at 10-cm Intervals with plastic boxes (2x2 cm). Paleomagnetic measurements were performed at the Geophysics Department, Stanford University, on a slow spinner-magnetometer (SSM-l). An alternate-field (a.f.) AC demagnetizer was used to partially demagnetize the samples. Instead of routinely demagnetizing all samples at one oersted (oe) peak-level, without recording the natural remanent magnetization (NRM), the RRM was always determined. Thereafter, specimens with unusually low In clinations, and those within or close to polarity events and boundaries, were partially demagnetized up to four times at Increasing peak-levels. This procedure was adopted because a constant level of demagnetization (In the normally used range of 100-150 oe) significantly re duced the angle of inclination of some samples, especially If normally magnetized. In addition, demagnetization levels in excess of 200 oe were sometimes required to eliminate secondary components of reversed specimens. An added advantage of treating samples under different mag netization levels Is the possibility of comparing their magnetic behavior. The paleomagnetic data were reduced and plotted with an IBM 360/65 computer (University of Southern California Computing Center) and the FORTRAN IV program given in Appendix II. PALEOMAGNETISM OP CORES Stability of Magnetization Earlier studies demonstrated unstable components of magnetization to be common in deep-sea sediments (Opdyke and others, 1966; Hays and Opdyke, 1967; Goodell and Wat kins, 1968; Opdyke and Foster, 1970) thus substantiating the need for partial demagnetization. Yet, few investi gations emphasized the variation of these components from core to core. One reason for this is the general failure to report NRM values in deep-sea reports; rather, the in clinations that are reported result mostly from demagneti zation of all samples in a core at standard peak-levels. Comparisons before and after removal of secondary magnetic components are then impossible. In the present study, up to four a.f.-demagnetizations were performed and the NRM of all samples was recorded. There is only a vague relationship between gross lithology and amount of unstable components. For example, £39-56, a radiolarian-dlatom clay almost throughout, was extremely stable. After cleaning with peak levels of 50-200 oe, none of the boundaries shifted and only one specimen (1290 cm; Appendix I) changed sign of inclination. 23 24 Some Inclinations even decreased by several degrees In response to Initial treatment. Other cores, although of similar llthology, required extensive demagnetization to reduce the dispersion of the Inclinations. E39-48 repre sents this group well; It is also predominantly clay, with generally less than 10 percent biogenous components, but the reduction in lnclination-scatter after cleaning is drastic. Figure 6 compares the confusing NRM values with the simplified and organized polarity log demagnetization produced in such cases. The behavior of Isolated samples, of comparable gross llthology, subject to Increasing a.f- demagnetlzation, again stresses the fact that similarity in gross composition can still result in different magnetic behavior (Fig. 7). There is, however, a certain predict ability in samples from the same core. Two specimens from £39-76 responded in the same pattern upon demagnetization (Fig. 7). It is also apparent that foramlnlferal oozes show a greater dispersion of inclinations than other sedi ments when the NRM is compared. Opdyke and Foster (1970), in an analysis of North Pacific cores, found a down-core decrease of magnetic resolution in most of their "red clay" cores. E39-67, a foramlnlferal ooze, behaved in a similar manner. A systematic decrease in inclinations with depth, such as noticed by Keen (1963), was discovered in E39-58 (compare also Fig. HE). An opposite trend occurred in E39-24 (see Figure 6 Comparison of magnetic inclination in E39-48 before and after a.f.- demagnetizatlon. 25 26 E 39 - 48 -90 INCLINATION (DEGREES) 0 +90 E x Q. LjJ o -90 ♦90 NRM NRM, 100-300o e Figure 7. Comparison of magnetic behavior of isolated samples after consecutive demagnetization under Increasing fields. M = intensity of magnetiza tion after demagnetization; M0 = untreated Intensity. E39-56 is a siliceous clay; E39-48 is a calcareous-siliceous clay; E39-76 is a calcareous clay; and E39-50 is a siliceous-calcareous clay. 27 • E 39--56 0-5 cm. • E 39--48 345 cm. :e 39--76 0-5 200 cm. ■ E 39--50 920 cm. i 1 ----1 ----1 ----1 i 1 i 1 ----1 r 200 400 600 PEAK ALTERNATING FIELD (oe) 29 also Fig. 11A), however, suggesting that changes In in clination with depth are local phenomena related to sedi mentary conditions. As observed by Harrison (1966), the mean angle of Inclination of most cores is lower than that of the ambient field today. For the localities involved in this study, inclinations between -60° and -70° are expected (Vestine and others, 1947)* The discrepancies between ambient and paleo-lnclinations become negligible, however, if the inclination mode of stable cores is considered, and if experimental values on inclination errors because of sedimentation are taken into account (Griffiths and others, I960; Rees, 1961). Opdyke and others (1966) demonstrated even closer agreement between both in two of their Antarctic cores, but these are probably exceptional ex amples. It appears that foramlnlferal oozes, even after proper demagnetization, exhibit consistently lower in clinations than other sediments during both reversed and normal sequences (compare Table 1 and Appendix I). This suggests correlation between sediment type and inclination that may be related to the percentage of silt and clay particles. Keen (1963), studying magnetic properties of North Atlantic cores, concluded that the largest propor tion of magnetic material was contained in the 22 to 44- micron fraction, magnetite being the primary contributor. The magnetic susceptibility of said size fraction was nearly ten times that of larger particles 30 Intensity of Magnetization Most cores have Intensities of magnetization of the order of 10“^ to 10“^ electromagnetic units (emu) (Figs. 8, 9; Appendix I). This agrees with results of previous Antarctic studies (Opdyke and others, 1966; Goodell and Watkins, 1968). One exception was E39-24, which had con siderably higher magnetization (10~^ emu; Appendix I). On an areal basis, no distinct trends were noted, but It is Interesting that the two westernmost cores (E39-22 and 24) had the highest overall intensities (Appendix I). Plots of intensity, llthology, and percent sand of some representative cores (Fig. 8) fall to show any trends. The contention that llthology correlates with intensity (Opdyke and others, 1966) is thus not corroborated by the present material. Moreover, foramlnlferal oozes gave no indication of lower intensities than other sediments (Fig. 8, Appendix I). In any case, it Is doubtful that the types or amounts of blogenous components directly in fluence magnetization intensities. Their role seems secondary, perhaps providing chemical microenvironments that influence the magnetic particles during settling and compaction, or masking the more Important silt particles. In several cores a definite inverse correlation exists between reversals and intensity of magnetization. Figure 8. Comparison of magnetic Intensity with gross llthology and percent sand of selected cores. The sandy fraction is predominantly blogenous In these cores. 31 CORE LENGTH (m) h 't h ' i 1 0 20 rri'i'm 40 60 6 - 8 - 10 - 12 - E39-22 CALC.-SILIC. CLAY E 39 - 40 CALC. OOZE % SAND «I0 n 11 > r1111111 .. ... . 0 20 0 20 0 20 % S A N D ■ o ' * i o - s i o - 4 K f * i o ' 4 i o " s emu E39-76 CALCAREOUS CLAY E39-50 S I L I C . ' C A L C . CLAY E39-56 SILICEOUS CLAY ro 33 The beginning of reversals are normally associated with the lowest Intensities (Fig. 9)* Ninkovich and others (1966), and Opdyke and others (1966) have stated this be fore. Furthermore, In a few cores, overall Intensities throughout reversed sequences are depressed compared to equivalent normal periods (Fig. 9). With the limited amount of Information at hand, however, one cannot be cer tain of a real relationship. And, lower Intensities dur ing entire reversed sequences would contradict the dynamo theory. Interpretation of Magnetic Stratigraphy The paleomagnetic time scale for the last 5.0 m.y. (Fig. 10) represents a compilation of Information gathered by many authors over a number of years. Results from studies on K-Ar dating and paleomagnetic measurements of lavas, paleomagnetic work on deep-sea cores, and Interpre tation of magnetic anomalies of oceanic ridges contributed to Its definition (Cox, 1969). An excellent chronological review of its development, problems, and future pos sibilities and limitations has recently been published by Watkins (1972). Controversies still exist concerning the proper nomenclature and duration of some events, in parti cular those of the Matuyama Reversed Epoch, but most major boundaries are now well established. Inclination plots of the cores under study, and Figure 9. Inverse correlation between Intensity of magnetization and reversals In representative sections of cores E39-76 and E39-50. Positive Inclinations correspond to reversed magnetlza tlon. 34 35 (emu) IN C L IN . (D E G R E E S ) INTENSITY -90 2- 4- E 39-76 6- 8- (m) E 39 - 50 Figure 10. The established paleomagnetic time scale. Mainly after Coz (1969) but Incorporating data from Hays and Opdyke (1967T and Opdyke and Foster (1970). 36 o Ll 01 o ro o 0 1 I I r " i ' W " i l r i rwrn^ O m i m m zr .i- M l ^ I ■ I f / J Z ^ Z k —I ^ H w 2 m i n POLARITY EVENTS 9RURRE? NORMAL EPOCH EPOCH 5 NORMAL GILBERT REVERSED EPOCH GAUSS NORMAL EPOCH MATUYAMA REVERSED EPOCH POLARITY EPOCHS their polarity logs, are shown In Figures 11A-11G. Ex cept for cores E39-40 (not demagnetized) and B39-63 (last sample demagnetized), Inclinations are a combination of NBM and demagnetized values. Appendix I gives all numeri cal paleomagnetlc data. Following Watkins' (1968, 1972) advice, all polarity events or deviations are recorded In the logs. It Is clear that microfossil control is essen tial to the interpretation of the present polarity logs. For this reason, In the present section reference is often made to faunal evidence that will be fully discussed only in the next chapter. Few of the many polarity events seen could be re ferred unambiguously to equivalent events in the establish ed scale. Situations like those reported by Watkins (1968) are common; he pointed to the usual occurrence of short- polarity events which are Inconsistent with known events and are to be expected, especially near polarity bound aries, due to animal redeposltlon. Nevertheless, a clear separation of two magnetic epochs, corroborated by blo- stratlgraphic control, was possible. Most cores commence with a erection of normal polarity, Interpreted here as mainly Gauss in age. But, careful evaluation of the fauna in the tops of the cores reveals that some oores also contain layers of Brunhes sediments in their upper portions. Some reversals are usually found in these Gauss sections. In six cores, the normally magnetized sediments Figure 11A. Interpretation of the magnetic stratigraphy In cores E39-22 and 24. Negative Inclinations cor respond to normal magnetization in the southern hemisphere. In the polarity logs, black indicates normal, white reversed magnetiza tion, and stippling refers to samples lacking a definite verti cal magnetic orientation. The actual numerical values are given in Appendix I. 39 INCLINATION (DEGREES) -90 0 +90 INCLINATION (DEGREES) -90 0 +90 (O to 3 < o E39-22 NRM,!00-800oe E x Q. l l i o l o co CO 3 < o E 39-24 NRM, 200-250oe Figure 11B. Interpretation of magnetic strati graphy in cores E39-40, 42, and 44. Note disconformities indi cated by faunal analysis. 41 OIPTM (n) INCLINATION (DECREES) -00 0 +00 INCLINATION (DEORCES) KoMMf 00 ♦ 00 f t- 4- E 3 9 - 4 0 NRM E 3 9 - 4 2 NRM, 8 0 -1 2 5 oe O I P T N I r I (O to INCLINATION (0E4NCCS) -00 0 400 Mammoth E 3 9 - 4 4 NRM, 1 0 0 -3 0 0 o« 4 s - ro Figure 11C. Interpretation of the magnetic stratigraphy in cores E39-48 and E39-50. 43 INCLINATION (DEGREES) -90 0 +90 Disturbed Koena Mammoth 3.32 my x 4- ui o E 39-48 NRM, 100-300 oe INCLINATION (DEGREES) -90 0 4 -90 CO 4- E x i- Q. I l l O UJ t o - E 39-50 NRM, 50-300oe ■> ■ p- Figure 11D. Interpretation of magnetic strati graphy in core E39-56. Question able position of Gilbert "b" event between about 6 and 8 m is sug gested by micropaleontological analysis and increased dispersion of inclinations. 4 5 E 3 9 - 5 6 NRM, 5 0 * 2 0 0 oe Figure HE. Interpretation of magnetic strati graphy in cores E39-58 and 63. The highly dispersed inclinations in E39-63 are chiefly due to the lack of demagnetization. 47 INCLINATION (DEGREES) E39-58 NRM, 12.5-150oe K A E N A DEPTH (m) INCLINATION (DE6REES) GILBERT?B-3.32my E 3 9 -6 3 NRM, l50oe ■&- oo Figure 11F. Interpretation of the magnetic stratigraphy in core E39-67. Several samples are missing in the upper 2 m. The disconformlty is indicated by the faunal analysis. 49 INCLINATION (DEGREES) 0 50 -3 .3 2 I IO-1 E 3 9 - 6 7 NRM, l5 0 -2 0 0 o e Figure 11G. Interpretation of the magnetic stratigraphy In core E39-76. Faunal analysis Indicates a Gauss-Matuyama hiatus. 51 DEPTH (m) 52 INCLINATION (DEGREES) +•9 2- 4 - 6 - 8- 1 0 - t { [------^ tfUYAWiA co Kaena Mammoth E39-76 NRM, 100-800 oe 53 are followed by reversed sections, which correlate with the Gilbert Reversed Epoch. One or more normal events are distinguished in them. The first cores (E39-22 and 24; Fig. 11A) do not penetrate beyond the Gauss Normal Epoch. Each contains short, reversed events that cannot be compared to any of the known Gauss events. Furthermore, faunal control re veals that both failed to reach the Kaena event. As the positive inclinations involved are extremely low and short, regional, non-dlpolar variations of the field could conceivably be the cause (Watkins, 1972). A number of samples in E39-24 virtually lacked vertical components. It is likely that these are also expressions of short ambient field variations. Since E39-24 has an extremely high sedimentation rate, even short deviations would re gister. Collection and laboratory-induced errors are un likely as cores and samples were carefully handled and the data follow reasonable patterns. Faunal redeposition is likewise ruled out; there are no reversed sequences nearby. Finally, both cores have the strongest overall intensities indicating that the deviations are not the result of resolution limitations of the magnetometer. The cores in the next group, E39-40, 42, and 44, contain varying amounts of Brunhes Normal Epoch sediments above Gauss age sediments. The large reversal between 140 and 180 cm in E39-40 is here thought to be the Mammoth 54 event. The nearly horizontal points above It are probably remnants of the Kaena event marked by unstable components. Unfortunately, this core could not be demagnetized. It Is reasonable to Interpret the normally magnetized sample at 440 cm as the Gilbert "a" event. Assuming constant sedi mentation rates, this sample would fall near the bottom of that event (Fig. 11B). The last, almost horizontal, normal data-polnt at 530 cm Is possibly a remnant of the Gilbert "b". Only proper demagnetization can clear this Issue. Core E39-42 contains a late Gauss-late Brunhes dlscon- formlty at about 300 cm, and Its Gauss section, as fossils show, failed to reach either of the known events. In con trast, E39-44 contains both the Kaena and Mammoth. The fit with the established chronology of the Gauss Is not satisfactory In this core, partially because most of the first two meters are Brunhes In age. This explains the Inordinate length of normal sediments above the events. The first 150 cm of E39-48 were not sampled due to severe coring-induced distortions. The remaining section leads through most of the Gauss (and both of Its events) into Gilbert sediments, with Gilbert "a" and "b" clearly developed. The splitting of Gilbert "b" is Interesting, since Opdyke and Foster (1970) found a split Gilbert Mc” event in one of their North Pacific cores. A split Gil bert "c" event has also been predicted from analysis of magnetic anomalies by Pitman and Helrtzler (1966). It is 55 possible that the spilt event In the present core (Fig. 11C) might actually be the Gilbert "o" but faunal content makes It unlikely. Future studies will be necessary to verify the nature of the Gilbert "c" event. The reversed point at 610 cm was demagnetized twice Insuring Its reality (Appendix I). £39-50, despite a long sequence of stable, normally magnetized samples that are, therefore, Interpreted here as Gauss, did not contain any reversals. Faunal activity must have blurred the record because sedi ments paleontologically equivalent In age to the events were penetrated. The three short-period normal events of the Gilbert section in E39-50 (Fig. 11C) are a matter of speculation. Repeated demagnetization confirms their magnetic reality (Appendix I). The two lower ones may have originated by sediment redeposition. Although 60 cm apart, they could still be within the limits of animal activity (Watkins, 1968). Both are therefore regarded as the Gilbert "a" event, which is substantiated by their fauna. £39-56 is of considerable interest since Its top contains the oldest surface sediments of the area. Its polarity is normal at top (double demagnetization shows this to be consistent and a trigger core sample, also normal, corroborates it; Appendix I), possibly represent ing the base of the Gauss. Gilbert sediments follow In which two normal events are distinguished: the first is 56 definitely Gilbert "a", but the second must be Gilbert "c\ since it contains the oldest radlolarlan faunas re covered by the cores. The absence of Gilbert "b" is odd. Between 5*5 m and 8 m, however, there is an unusual scatter of inclinations that demagnetization failed to remove (Fig. 11D). Conceivably, Gilbert 'V sediments were re worked into these horizons losing most of their normal polarity. The only compatible Interpretation of biostrati graphy and polarity in E39-58 is to regard the predominant ly normal sequence as upper Gauss, and the subsequent, re versed portion as the Kaena event. The two normally magnetized points at 460 and 570 cm represent, then, the remainder of the middle Gauss that separates the two events. There is a noticeable decrease in quality of magnetic data below about 260-280 cm in this core (Fig. HE) which is represented as a remarkable decrease in magnetic intensity (Appendix I), and coincides with the beginning of the reversed section. An inordinate pro portion of small-sized foraminlfers in the first 330 cm, reflected in the distribution of the sand-sized particles, implies that this core be treated with suspicion. This section possibly is the result of turbldlte deposition. In core E39-63 (Fig. 11E) only the last sample could be demagnetized. The inclinations, at times shallow and dispersed, suggest magnetic Instability that demag- 57 netlzatlon would have removed. As it is, the record repre sents chiefly Gauss sediment with one large, reversed event that mlcropaleontologlcally correlates with the Mammoth. The two normal data points within the event probably would have changed sign after demagnetization or are the result of faunal activity. Presumably, Kaena sediments are represented by the erratic Inclinations of the center part of the core. The last sample, definitely reversed after a 150-oe treatment, corresponds to the top of the Gilbert Epoch. E39-67 (Fig. IIP) Is particularly interesting des pite several missing samples and overall poor magnetic quality. The first 300 cm are Gauss in age and two, If not three, reversed events can be distinguished here that best correlate with the Kaena and Mammoth. Subsequently, Gilbert sediments follow In which Gilbert "a" and "b" are clearly delineated. Below Gilbert "b", at 570 cm, a large hiatus separates underlying middle Miocene sediments. The contact is vague and mixing of both ages takes more than 110 cm (Fig. 11F). The inclinations continue to be re versed to 650 cm, where another normal event occurs. Thereafter, reversed sediments down to 800 cm are followed by a normal portion of almost 200 cm. Paleontological control does not rule out any further hiatuses, however, and sedimentation rates may have varied. Since the whole core is a foramlniferal ooze and contains some indices, the portion below the unconformity adds to the definition of Miocene polarity sequences. It probably represents the oldest paleomagnetlcally dated sediments recovered from the subantarctlc region. The last and northernmost core, £39-76, in contrast to its deceptively simple polarity log, again is difficult to interpret. The first sample is reversed but its rela tionship to the established polarity scale is questionable because three samples from the trigger core, which con tained the actual sediment surface, show no sign of re versals (Appendix I). Faunal control shows that the re versed event at 200 cm in reality corresponds to a shortened Matuyama Epoch, above which Brunhes sediments are found. A hiatus separates this portion of the Matuyama from the Gauss below. At 430 cm begins the Kaena, and at 970 cm the Mammoth event (Fig. 11G). A generalized correlation with the magnetic scale of the discussed cores is attempted in Figure 12. The most striking aspect of this correlation is the constancy with which middle to upper Gauss sediments are exposed in this area. As stated before, some cores contain veneers of Brunhes, or mixings of Brunhes and Gauss in their tops but, except for the very obvious cases, these Brunhes core tops are correlated with Gauss in Figure 12. The remark able uniformity in ages exposed in this area requires that a large-scale mechanism commenced its action almost instan- Figure 12. Generalized correlation of all polarity logs with the magnetic scale. Only major hiatuses and mixed sections have been Included here. For details see blostrati- graphlc Interpretations of each core In Figures 15A-H and 16. 59 . 0 9 1 _L_ IM _ l_ LENGTH OF C O R E S (m) C D 0> « N O I I ______I ______ I _____I o cm; i s flI KAENA MIDDLE MIOCENE( >ia si i GAUSS MATUYAMA £ EPOCH Millions of Yeors 09 3 9 -2 2 3 9-24 39-40 39-42 39-44 3 9 -4 8 39-50 3 9 -5 6 3 9 -5 8 39-63 39-67 taneously throughout the region. The explanation given by Watkins and Kennett (1971, 1972), which supposes an in crease of bottom-water velocities, is therefore highly plausible; greater attention will be devoted to it in the sedimentation section. One final statement regarding paleomagnetic strati graphy: unless ''ideal" cores are selected, and many of the previously studied cores are just that (Opdyke and others, 1966; Hays and Opdyke, 1967; Hays and others, 1969), it is almost impossible to correlate with the established polarity scale without excellent faunal control. Studies of large numbers of cores, such as that by Goodell and Watkins (1968) can only give very approximate, subjective results. Even with the aid of mlcrofosslls major dif ferences of interpretation can follow. This is shown by comparing Figure 12 and a similar correlation by Watkins and Kennett (1972) of parallel cores taken during Eltanln cruise 39. Conversely, if "ideal" cores are always selected for studies, the complexities of the "normal" sedimentary record tend to be overlooked, and existing ideas will be reinforced at the expense of innovations (Watkins, 1972). An excellent illustration of this is the interpretation of Gauss inclination plots before the general acceptance of two Gauss events in the established scale. Some authors did not report two reversed events in their Gauss polarity logs, despite presence of both events in the corresponding inclination plots. I BIOSTRATIGRAPHY OF CORES Ranges of Selected Radlolarla Late Neogene radiolarian Indices of antarctic to subantarctlc regions afford excellent means of correla tion with the paleomagnetlc time scale (Opdyke and others, 1966; Hays and Opdyke, 1967; Bandy and others, 1971)* Based on the ranges and upper limits of some Indices, Hays (1965) and Hays and Opdyke (1967) proposed six radiolarian zones comprising the Gilbert to Brunhes Epochs. Bandy and others (1971) later subdivided three of these (Table 2). The two oldest of these zones (Upsllon and Tau) were ex amined here In detail because they represent most of the sediments In the present cores. It soon became clear that both could not be readily applied— the defining species were either confusing taxonomlcally, ranged beyond their stated upper limits, or did not appear at all. Obviously, a more practical Gllbert-Gauss zonatlon was required. Be fore proposing such a zonatlon, however, the most useful Indices and datum planes based on them will be reviewed. Most of the datum planes are evolutionary events that transcend the present latitudes. Consequently, they serve as a basis for world-wide correlations. 65 Table 2. Previous antarctlc-subantarctic planktonic zones Subzone Characteristic species Approximate paleo* magnetic age of upper zonal lllU (i»y.)__ EADIOLAHIA Omega Psl Chi Phi Upsllon a a b c d Spongoplegma antarctlca. with Saturnulus planetes and Theoconus zancleus S. antarctlca alone Stvlatractus unlversus S. planetes, Pterocanlum trllobum Eucvrtldlum calvertense Desmospvrls snonglosa. Helotholus vema Prunopvle titan, IflLgfrBOgfrftlutt £E&B&e Oroscena (digitate), 0. carolae Cyrtocapsella tetraptera. Theocvrtls redondoensls Latest Brunhes 0.4 0.7 1.8 2.4 Upper Gauss Upper Gilbert Upper Gilbert o\ ■ e - Table 2. Previous antarctlc-subantarctic planktonlc zones (continued) Zone Subzone Characteristic snecles Approximate paleo- magnetlc age of upper zonal limit (m.v.) EADIOLAHIA Tau a Trlcerasoyrls so. Gilbert "b" b Ommatocamoe hughesl. Cannartlscus marvlandicus Gilbert V FORAMINIFERA Globorotalia trun- catullnoldes Zone Same sp. G. Inflata Zone Same sp. 0.2 (*) G. nuncticulata Zone Same sp. 0.65 (*) (*) Extrapolated age. References: Hays, 1965; others, 1971 Hays and Opdyke, 1967; Hays, 1970; • Kennett, 1970; Bandy and O n i Table 3 lists selected radiolarian Indices, datum planes, and approximate upper limits relative to the paleo- magnetic scale. Some limits are of migratory nature, others may be due to reworking. Comparisons with those given for the same species by Hays and Opdyke (1967) and Bandy and others (1971) shows some discrepancies (Fig. 13), which probably result from the larger amounts of material studied here. Figures 14A-H show the ranges of the faunal indices in most of the paleomagnetically dated cores. Ad ditional faunal-range data can be found under Interpreta tion of Blostratigraphy (Fig. 16). Plate 1 illustrates many of the species on Table 3; references to all radlo- larlans mentioned appear in Table 4. The most important species, from oldest to youngest, are: 1. Stlchocorvs delmontense. Although not found in the present material, it is included here because it occurs in the bottom (1750 cm) of E14-8, a Pacific- antarctic core (Casey, 1972), at an estimated time of 5*2 m.y.b.p. It will surely become a useful index when addi tional older sediments are recovered. It serves well for Miocene correlations in many regions, and was originally described from southern California (Campbell and Clark, 1944). In the tropics, it first appears in the early Miocene Calocvcletta Virginia Zone (Riedel and SanfHippo, 1971). Its upper limit overlaps the first appearance of its direct descendent, S. peregrlna. by amounts that 67 Table 3. Evolutionary and non-evolutlonary planktonlc events encountered In this study Approximate paleomagnetic Snecles Nature of event age (m.y.) Stlohocorvs oeregrlna first appearance 5.0 ? Globorotalla lnflata lnflata first appearance A.3-3.4 Lamnrocyclas hetero- noros first appearance 4.2 Globorotalla mlozea mlozea extinction 4.2 G. truncatullnoldes first appearance 3.3 Snhaeroidinella de- hiscens lmmatura first appearance Mammoth event S. dehlscens dehlscens first appearance Top of Mammoth Pullenlatlng obll- aulloculata first appearance Middle Gauss Oroscena (digitate) S P . extinction ? 2.7 Theocyrtis redondo- ensls extinction ? Kaena event CannartlscuB marv- landlcus extinction ? Upper Gauss Cyrtocapsella t?3tTapt8.r& extinction ? Upper Gauss Globorotalla mlozea conoldea and G. mlozea snherl- comlozea extinction 2.6 68 Table 3* Evolutionary and non-evolutlonary events encountered In this study planktonic (continued) Suedes Nature of event Approximate paleomagnetlc ace (m.y.) G. nunctlculata Dunctlculata and G. nunctlculata nadana emigration 2.6-2.5 Stlchocorvs oereerlna. Frunonyle titan, and Lychnocanlum Krandg. extinction 2.5 Clathroovclas bl- S.QXfl.lff extinction 1.8 (*) Stvlatractus uhiyergug extinction 0.4 (*) (*) Hays, 1971. Figure 13* Generalized ranges of radiolarian and planktonic foramlnlferal In dices In the present area and In previous work. Except where speci fied otherwise* the following re ferences were used: Eq. Pacific = Hays and others, 1969; £9* Pacific (V24-59) = Casey, pers. comm., and Bandy and others, 1972; N. Pacific = Olsson and Goll, 1970, Olsson, 1971; E14-8 = Casey, 1972, and Bandy and others, 1971; Southern California = Casey and others, 1972; Antarctic region, Other antarctic cores, and N. of P.F. (north of Polar Front) = Hays, 1965, Hays and Opdyke, 1967* Hays, 1970, Hays, 1971, Bandy and others, 1971; South Pacific-Previous antarctic zonatlon = Kennett, 1969, 1970; Low latitudes = Berggren, 1968; Philippine Sea = UJlie' and Mlura, 1971; Jamaica = Robinson and Lamb, 1970. 69 W IT H MAGNETIC SCALE ttl LANO- EASED m U J MATUYAMA M A G N E T I C E P O C H S A G E (millions of yoo rs ) P O L A R I T Y ( / > s * * $ o ^ h n P t! h m Co Pacific (V 24-50) • Savtlwn California ^ THIS STUOY Eo N ellie N Pacific Saatliarn California<f>tl -T H IS STUOY f ArnsrvffPieiL » THIS STUOY — N. Pacific I • THIS STUOY • Other Antarctic cmw Eo Pacific ( V t4-S 9) — Saatharn California M l • — THIS STUDY O lN f Antarctic in w — Co. Pacific (VS4-5S) - * THIS STUOY ■ Other Antarctic TNI I STUDY — Other Ant. caraai N. of PC* n t n —caa R mwMN i : i • I : I : if ."i •A ntarctic Naslaa - E t Pacific — S . DELMONTENSE S . PEREGRINA Digitate OROSCENA 8 Q CAROLAE L. HETEROPOROS P TITAN L. GRANDE C. BICORN IS E. CALVERTENSE S. UNI VERSUS TH IS STUOY - H . S U I I I * ' 1 ’ IS. l » I W ».!■> ■ THIS STUDY ■ N. S M lfla *" •T H IS STUDY ■ H. Pm HN 1 1 1 __________ • THIS STUDY s. H m iik - P fM lM t S ukm M M IIt ZWMtlM — H. Pm UU 1 1 1 THIS STUDY THIS STUDY » « » » - 8 Pacific • Province : _______N. PanIfln 01 THIS STUDY Santh Paalfla-Ptavtaca Saha*. Low inWaAcn................... ■ ■ ■ ■ WZ T iy s STUOY (1 0 -TOM THIS STUOY(ESS-Tt) ■■■*» Phlllntlaa S n Eo to a lfla # - - - Nntaarhnaf——- Ca fWcWle it) hldCC THIS STUOY (ESS»Tt>— E f Pacific =r THIS STUOYtnS-TSIH t, SIMM t< S»«HI«__________ THIS STUDY ICSS-TS) kl«tm a . H h IIIc i i i G. MIOZEA MIOZEA G. MIOZEA CONOIDEA G. MIOZ. SPHERICOMIOZ. G. PUNCTICUL. PUNCT. G. PUNCTICUL. PADANA G. INFLATA INFLATA G. TRUNCATULINOIDES P PRIMALIS S. DEHISCENS P OBLIQUIL. OBLIQUIL. G. TOSAENSIS P . OBLIQUIL. FINALIS o m iE — r r - r * » U P P E R M I O C E N E I ^ > C35 P L I O C E N E | P L E I 5 T 0 - H O L O C EPOCHS 0 2 . R A D IO LARI A FO RA MINI FERA Figure 14A. BioBtratigraphic Interpretation of E39-76. Note that core is almost barren due to solution. 71 E 39 - 7 6 G A U S S Almost borren foram iniferol cloy POLARITY a EPOCHS L I T H O L O G Y no zZ 25 DM » t b. MIOZEA CONOIDE A- G . TRUNCATU N 19_________ ffTRUNCATUL 2 -N 2 3 ? G. TR U N C A TU LIN O ID ES G. TOSAENSIS S. DEHISCENS IMMATURA S. DEHISCENS DEHISCENS P. P R IM A L IS P. OBLIQUILOCULATA s s. G M IO ZEA CONOIDEA b. SPHERICOMIOZEA G. INFLA TA INFLATA G. INFLATA TRIANGULA G. CRASSAFORMIS s.I. G. PUNCTICULATA PADANA P. OBLIQUILOCULATA FINALIS G. cf. CRASSULA VIO LA PROPOSED ZONES BLOW'S ZONES (1969) r T o P L I 0 C E N E PL.- HOLOC. EPOCHS o> ro Figure 1AB. Biostratigraphic interpretation of E39-67. 73 E 3 9 - 67 MIDDLE MIOCENE G LBERT GAUSS Foraminiferal Ooze POLARITY 8 EPOCHS LITHOLOGY .TYPIST ^TYPICAL LILLBURNI AN i z z i 1 r~ o 3 6. MIOZEA MIOZEA G. TRUNCATULINOIDES G. INFLATA s.s. G. MIOZEA SPHEmCOMIOZEA G. PUNCTICULATA ^ ¥ f CUUATA G. CRASSAFORMIS s i G . cf. CRASSULA VIOLA G. DECORAPE RTA G. WOOD I s. s. G. NEPENTHES 0. SUTURALIS P . GLOMEROSA CIRCULARIS UNZONED G .M .M J g .mioz.c o n 1 g .m . c .-g . trun. y G .x FORAM. ZONES ” TONGAR-KAPITEAN OPOITIANI N. Z. STAGES o> ro Figure 14C. Biostratigraphic Interpretation of E39-63. The spotty occurrence of some radlolarlans, particularly the warmer, upper Miocene forms, may be the result of the extreme scarcity of radlolarlans In this dominantly calcareous core, or Is due to reworking. It Is of Interest, however, that the occur rence of these forms generally coincides with warmer intervals (Fig. 18). 75 m CM < 0 i 0> CM G A U S S Calcar. Clay — Foram. Ooze POLARITY 8 EPOCHS LITHOLOGY G. TR U N C A TU LIN O ID ES G MIOZEA CONOIDEA 6. MIOZEA SPHERICOMIOZEA G. IN FLA TA s s. G. PU NCTICULATA pADANA G. CRASSAFORMIS P. T ITA N L. GRANDE o (DIG ITATE) u CAROLAE S. PEREGRINA E. CALVERTENSE C. BICORNIS L. HETEROPOROS C. TETR A PTER A C. M ARYLANDICUS C. MARGATENSIS D. SPONGIOSA T. REDONDOENSIS L. M ARITALIS FORAM. ZONES G. M.C.Z. |G.MC.-GTRUNC.Z.|GlTRUNC. Z S. P E R E G R .- L. HETEROP ZONE J C .B IC .Z .l RAD. ZONES — | — i ---1 --1 — | — » — | ---- ------- ro T o < 3> F O R A M IN IF E R A RADIOL ARIA Figure 14D. Blostratlgraphlc Interpretation of core E39-58. At about 300 cm the lithology changes from cal careous ooze (usually oontalnlng from 40-60 percent sand) above to calcareous clay below. Since the foramlnlfera In the upper portion are abnormally small, It is possible that this portion constitutes the flne-fraction of a turbidite. The change in lithology is reflected in a marked change in magnetic in tensity (Appendix I). 77 E39-58 G A U S S m m Calc. Clay - Foraminiferal Ooze POLARITY a EPOCH L IT H O L O G Y G. TRUNCATULINOIDES G. INFLATA S. S. G. CRASSAFORMIS S. L. G. MIOZEA CONOIDEA G. PUNCTICULATA S. L. G. cf. CRASSULA VIOLA G. MIOZ. CON - G.TRUNCAT Z. ^G. TR FORAM. ZONES 1 1 i i 1 1 ^ IN > O C O Figure 14E. Blostratigraphic interpretation of E39-56. This core reached the oldest radiolarian sediments of the study. 79 E 39-56 B O - E Siliceous Cloy POLARITY LITHOLOGY a EPOCHS PRIM ITIVE T Y P IC A L G INFLATA * • . G. PUNCTILCUL ATA s. I ft u m 7 P A CONOIOEA b. " l U i t # SPHERICOMIOZEA G. MIOZEA MIOZEA P . TITAN S. PEREGRINA L. GRANDE E. CALVERTENSE C. BICORNIS L. HETEROPOROS 0. (D IG ITA TED ) 0. CAROLAE C. TETRAPTERA C. MARYLANDICUS D . SPONGIOSA T. REOONDOENSIS C . MARGATENSIS S. PLANETES P TRILOBUM L FURC AS PICUL ATA E ACUMINATUM L. MARITALIS CALOCYCLAS tp. S. PEREGRINA ZONE x X S. PEREGR.-L. HETEROP. ZONE X X a > T X X X RADIOL. ZONES 00 o FORAM. RAD IOLAR IA Figure 14F. Biostratigraphic interpretation of E39-48. 81 E 39 - 48 f G I L B E R T I GAUSS ___ E 3_ _ f... - S iliceo u s-C o lco rco u s Cloy Calcareous C/ay POLARITY & EPOCHS L IT H 0 L 0 6 Y ■ “ ** ““ • * • * • i ■ * ■ • * m m “ m PRIM, f t TYPICAL TYPICAL ONLY m m 6. M. M IO ZEA |S. PEREGRINA Z. § 'I s I 3 I 0) I I G. TRUNCATULINOIDES G . INFLATA s. s. r u m 7 PA CONOIDEA G. MIOZEA SPHERICOMIOZEA G. MIOZEA MIOZEA G . PUNCTICULATA pa*DANA G. CRASSAFORMIS S.L G. cf. CRASSULA VIOLA P . TITAN E.CALVERTENSE S. PEREGRINA L. GRANDE C. BICORNIS 0. (D IG IT A T E ) L. HETEROPOROS C. MARGATENSIS S. PLANETES P . TRILOBUM THOLONIDS [ g . MIOZEA CONOIDEA Z0NE|G.M.C.-G.TRUN.ZG.TR.Z. S. PEREGRINA - L. HETEROP. ZONE vC.BIC? 7 T T 3 ® U PPER 1 --- M IO CENE I o> T FORAM. ZONES RADIOL. ZONES EPOCHS ro 00 K> FORAMINIFERA RADIOL ARIA Figure 14G. Biostratigraphic interpretation of E39-40. 83 E 3 9 - 4 0 GAUSS Foraminiferal Ooze 5 P O LA R ITY 8 EPOCHS LITHOLOGY X G . TRUNCATULINOIDES G . INFLATA s.t. G . PUNCTICULATA puJJcT^ CONOIDEA SPHERICOMIOZEA G . MIOZEA \ X E. CALVERTENSE C. BICORNIS L. HETEROPOROS P. TITAN L. GRANDE P. TRILOBUM S. PLANETES G . MIOZEA CONOIDEA Z.|G.M.C.-G.TRU^ U NZONED X T 3 PISTON CORE — I ------ * T T ro i FORAM. ZONES RADIOL. ZONES TRIGGER CORE m O g f O 00 FORAM. R A D IO L A R IA Figure 14H. Biostratigraphic interpretation of E39-22. 85 Latest GAUSS C a lc .— Siliceous clay m o j co I ro ro G. TRUNCAT. Z. C. BICORNIS Z. _ _ l | | 3 ro POLARITY a EPOCH LITHOLOGY G. TRUNCATU LI NODES G. INFLATA s.s. L. HETEROPOROS C. BICO RNIS E. CALVERTENSE THOLONIDA D. SPONGIOSA FORAM. ZONE RADIOL. ZONE 00 o \ FORAM. RADIOLARIA probably vary In different climatic zones. In the ant arctic area S. delmontense Is restricted to sediments older than 4.6 m.y. In the Equatorial Pacific (oore V24-49), however, It Is found almost as high as the base of Gilbert "a" (Casey, pers. comm.). In the North Pacific It has not been found In horizons as old as middle Gilbert (Hays, 1970), yet In southern California It slightly overlaps the Lamprocvolas heteronoros datum plane (Table 3). As shown In the discussion of the latter species, this datum Is tentatively placed near the bottom of Gilbert "b" at about 4.2 m.y.b.p. It seems that the ultimate extinction of S. delmontense occurred first In the present area (and per haps In the North Pacific), later In the temperate Pacific, and finally in the Equatorial Pacific. 2. S. nereerlna (PI. 1, figs. 1, 2) is an excellent Gilbert to Gauss Index that evolved during the upper Miocene from S. delmontense (Sanfllippo and Riedel, 1970), and has been reported from the following localities and ages: Gilbert to Gauss sediments of the North Pacific (Hays, 1970) and the Equatorial Pacific (Hays and others, 1969); upper Miocene-Pllocene strata of southern Cali fornia (Casey and others, 1972); seemingly Gauss strata of LeCastella, Italy (Nalcagawa and others, 1971); the Tabianian (early Pliocene) of Italy (Riedel and Sanfllippo, 1971); upper Miocene DSDP drillings (Riedel and Sanfllippo, 1971), and many other sections of equivalent age. Theyer 86 Table 4. Radlolarlan and planktonic foraminlferal reference list RADIOLARIA Oalocyclas margatensls Campbell and Clark, 1944 OalocvclaB b p . Calocycletta Virginia (Haeckel). 1887, Cannartlscu? marylandlcus Martin, 1904 Clathrocycla8 blcomls Hays, 1965 Cyrtooanaella tetraptera Haeckel, 1887 P9810flpyrl3 SPOQfilflfia Hays, 1965 4 Eucvrtldlnm acuminatum (Ebrenberg), 1844 E. calvertense Martin, 1904 Helotholus vema Hays, 1965 Lamprocyclas heteroporos Hays, 1965 Lamprocyclas marltalls Haeckel, 1887 Llthamphora furcasplculata Popofsky, 1908 Llthellus nautlloldes Popofsky, 1908 Lychnocanlum grande Campbell and Clark, 1944 Ommatartus penultlmus Riedel, 1957 Oroscena carolae Friend and Riedel, 1967 Oroscena ££. (digitate) Prunopyle titan Campbell and Clark, 1944 Pterocanlum prlsmatlum Riedel, 1957 P. trllobum Haeckel, 1862 Satumulus planetes Haeckel, 1887 Snongaster pentas Riedel and Sanfllippo, 1970 Spongoplegma antarctlca Haeckel, 1887 Stlohocorys delmontense (Campbell and Clark), 1944 a. ttsjegrlna (Hiedel),1953 Stylatractus unlversus Hays, 1970 Spcngotrochus glaclalls Popofsky, 1908 Theocalyptra blcomls (PopofskyJ, 1908 Theocyrtls redPB.dOEjafila Campbell and Clark, 1944 PLANKTONIC FORAMINIFERA Candelna nltlda d'Orbigny, 1839 Globlgerlna bulloldes d'Orbigny, 1826 a* decoranerta Takayanagi and Salto, 1962 G. nepenthes Todd, 1957 G. woodl voodl Jenkins, i960 G. woodl connects Jenkins, 1964 89 Table 4. Radlolarlan and planktonic foramlnlferal reference list (continued) PLANKTONIC FORAMINIFERA Globoquadrlna altlsplra (Cushman and Jarvis), 1936 Globorotalla aemlllana Colalongo and Sartoni, 1967 G. crassacrotonensls Conato and Follador, 1967 G. orassaformis Galloway and Wissler, 1927» s.l. crassula viola Blow, 1969 ” G. a£. crassula viola Blow, 1969 G. crassula conomlozea Kennett, 1966 G. lnflata lnflata (d Orblgny). 1839 G. lnflata trlangula. n. subsp. G. margarltae Bolll and Bermudez, 1965 £,. mayerl maverl Cushman and Blllsor, 1939 G. merotumlda Blow and Banner, 1965 G. mlozea mlozea Finlay, 1939 G. mlozea conoldea Walters, 1965 G. mlozea sanhoae Blzon, 1965 G. mlozea snherlcomlozea Walters, 1965 G. punctlculata ounctlculata (Deshayes), 1832 G. punctlculata padana Dondi and Papettl, 1968 G. tosaensls Takavanagl and Salto, 1962 G. truncatullnoldes (d'Orbigny), 1839 5.. tumlda turn Ida (Brady). 1877 £. tumlda pieSlotumlda Blow and Banner, 1965 G. subscltula Conato, 1964 Urbullna suturalIs Bronnlmann, 1951 Praeorbullna glomerosa circularIs (Blow), 1956 Pullenlatlna obllaulloculata obllqulloculata (Parker and Jones), I865 P. obllqulloculata flnalls Banner and Blow, 1967 P. primalIs Banner and Blow, 1965 Sphaeroldlnella dehlsoens dehlscens (Parker and Jones), 1865 S. dehlscens lmmatura Cushman, 1919 jSphaeroldlnellopsls subdehlscens (Blow), 1959 Consult Campbell and Clark (1944), Riedel (1958), Hays (1965, 1970), Friend and Riedel (1967), and Riedel and Sanfllippo (1970) for radlolarlan taxonomy. See Parker (1967)* Blow (1969), and Jenkins (1971) for planktonic foramlnlferal taxonomy. 90 (1972) had, for the first time, recorded it from high, southern latitudes. It can only be stated approximately when, in terms of the magnetic soale, its evolution from §L. delmontense occurred. In core £14-8, §.. delmontense is found at 1750 cm (Casey, 1972). The paleomagnetics of this level is unknown; extrapolation, assuming constant sedi mentation rates, gives an approximate age of 5*2 m.y. that corresponds to latest Epoch 5* The bottom of E39-56, with an age of 4.6-4.7 m.y. (immediately below Gilbert "c"), contains the oldest radlolarians of the present material. There, §.. delmontense no longer occurs and S. peregrins is fully developed. Consequently, the first evolutionary appearance of the latter, and the extinction of the former, took place between about 5.2 and 4.6 m.y.b.p. (be tween the top of Epoch 5 and a level Just below Gilbert "c"). In the North Pacific, in a core that reaches be tween Gilbert Nb" and "c", Hays (1970) indicated that S. peregrins was still present. In V24-59 (Equatorial Pacific) S. neregrlna and S. delmontense overlap during the middle and lower Gilbert (Hays and others, 1969; Casey, pers. comm.), but the transition does not take place within the core. In the upper Miocene Pliocene section of Malaga Cove (southern California), the transition is found in the Mohnian (upper Miocene) Valmonte diatomite, considerably below the evolutionary appearance of Lamprocyclas heteroporos. a species discussed below. 91 Thus, It can be assumed that the first appearance of S. peregrine was a synchronous evolutionary event. If so, an excellent datum plane (S. peregrine datum) can be based on It (Table 3, Fig. 13)* Its paleomagnetlc age Is latest Epoch 5 to earliest Gilbert, here arbitrarily placed at about 5*0 m.y.b.p. Since the S. peregrlna datum also defines the bottom of the tropical upper Miocene S. peregrlna Zone (Riedel and Sanfllippo, 1971), the bottom of this zone should have an equivalent magnetic age. The upper limit of S. peregrlna occurs In the upper Gauss, above the Kaena, In cores where both events are recognizable (Figs. 14F, G). Due to the difficulties In estimating sedimentation rates, this Is arbitrarily placed at about 2.5 m.y.b.p; this Is consistent with Its extinc tion in the North Pacific (Hays, 1970), the Equatorial Pacific (Hays and others, 1969; Casey, pers. comm.) and In southern California (Casey, 1972). The S. peregrlna ex tinction datum plane, therefore, constitutes another synchronous radlolarlan event (Table 3» Fig. 13)* In cores that only penetrated the uppermost Gauss (E39-22, 24, and 42), this species is absent (Fig. 16). 3. Oroscena bp. (digitate) and Oroscena carolae (PI. 1, fig. 7), are common and distinctive Gilbert elements. Friend and Riedel (1967) originally discussed the potential value of orosphaerids for Cenozoic correla tions. Bandy and others (1971) found both species in 92 Gilbert sediments of antarctic core E14-8 and noted that their upper limit coincided with the upper Gilbert. In the present study, both species are abundant in lower to middle Gilbert (Fig. 13), but also continue Intermittently into the Gauss of some cores (Fig. 14C). These could h&ve been reworked, however, and at present their upper limits are left undefined. Since they are warm to temperate species, their disappearance from these latitudes is probably related to shifts in paleocllmates. Their large, conspicuous shape makes them excellent guide fossils. 4. Lamprocyclas heteronoros is a predominantly middle Gilbert to Gauss index whose evolution from Calocyclas margatensls in lowest Pliocene (Delmontian) beds of the Malaga Cove section, southern California, has been documented by Casey and others (1972). Both species, and some transitional forms (PI. 1, figs. 12-16) similar to the ones from Malaga Cove, begin to appear during the Gilbert "b" event in E39-48 and Just above this level in E39-40 (Figs. 14F, G). Isolated, typical specimens (pos sibly contaminations) are first found at about 1300 cm in £39-56; abundant specimens commence at 800 cm and above (Fig. 14E), where Gilbert "b" should have been. In the North Pacific it occurs below Gilbert "b" in V21-148, where the core becomes barren. Unfortunately, Hays (1970) did not comment on the morphology of specimens at this level. Casey (pers. comm.) found L. heteroporos in V24-59 93 (Equatorial Pacific) appearing for the first time In the upper Gauss. This could be climatically conditioned. Even though It cannot be demonstrated as clearly as In the Malaga Cove section, It Is likely that the first evolu tionary appearance of this species took place between Gilbert "c" and "b" In the present area and also In the North Pacific. Consequently, a third datum plane, useful In cold areas of both hemispheres, Is based on this event (Table 3, Fig. 13). Pending further study, a paleo- magnetlc age of 4.2 m.y. Is given to It. Extrapolation of Hays' (1965) original data shows that the upper limit of this species correlates with the top of the Gauss in VI6-66, a subantarctlc core. Employing the boundaries of Hays' zones In the other cores, which are not dated paleo- magnetlcally, to correlate Its upper limit, It would cor respond to the Gilsa (Olduval) event (Casey, 1972). This would then coincide with Its extinction In the northern and tropical Pacific (Hays, 1970; Casey, pers. comm.). Further study Is needed, however, before Its disappearance from the present area can be employed with confidence. 5. Prunopyle titan (PI. 1, fig. 3) and Lychno- canlum grande are two useful Gilbert to Gauss Indices. Both have Identical upper limits In the upper Gauss, above the Kaena event (Fig. 13), coincident with the S. peregrlna extinction datum. Remarkably, this extinction also occurs at the same level In E13-17 and E13-3 (Hays 94 and Opdyke, 1967; Bandy and others, 1971) if their In clination plots are reinterpreted to Include two events In the Gauss Epoch. In addition, both species are found In upper Miocene to lowest Pliocene sections of southern California (Campbell and Clark, 1944; Bandy, 1967; Ingle, 1967; Casey and others, 1972). In core V24-59 (Equatorial Pacific) both also become extinct in the upper Gauss (Casey, pers. comm.). The P. titan and L. grande extinc tion data, then, are two other radlolarlan events of major importance (Table 3» Pig. 13)* There Is a reduction In abundance of both species In the upper Gilbert. This is most pronounced In L. grande. 6. Clathrocyclas blcornls. easily recognized when typical (PI. 1, fig. 5) is present in Gilbert to lower Matuyama antarctic subantarctlc sediments (Hays and Op- dyke, 1967). Although not found outside this region, its consistent extinction at about 1.8 m.y.b.p. (Hays, 1971)» constitutes a regional datum plane (Table 3* Pig. 13). Hays (1971) has given unquestionable proof of the con stancy of its upper limit (based on six paleomagnetically dated cores). Sometimes, however, this species is found as a thin walled variety that resembles Theocalyptra bi- oomla. a subantarctlc form living today (Riedel, 1958); this relationship needs further evaluation. Since C. bl cornls becomes extinct at what is generally conceded to be the Pliocene-Plelstocene boundary, it serves a similar 95 purpose as Pterooanlum nrlsmatlum In the tropics (Hays and others, 1969)* 7. Bucyrtldlum calvertense (PI. 1, fig. 9) is probably restricted to sediments older than about 2.0 m.y. (Hays, 1971) and is common in Gilbert-Gauss cores. By itself, however, its upper limit is not reliable. It lives today in the North Pacific (south of 40° N; Hays, 1970) and occurs, possibly reworked, in core tops north of the Polar Front as a thin walled variant (Hays, 1965)* Such forms are seen also in Brunhes sediments of the pre sent area, but these, too, may be reworked. Thus, unless corroborated by other indices, little confidence can be placed in its disappearance from antarctlc-subantarctic regions below the Gllsa event (Hays, 1971). 8. Stylatractus universus. a species that was not studied, ranges into the Brunhes Epoch. There is suf ficient evidence to demonstrate that it became extinct on a world-wide basis at about 0.34-0.4 m.y.b.p. (Hays, 1965; Opdyke and others, 1966; Hays and others, 1969; Hays, 1970; Hays and Ninkovich, 1970; Hays, 1971). A final, widely applicable datum plane is based on it (Table 3, Fig. 13). Radlolarlan Zones The zonatlon proposed below and in Figure 15 is based on five of the radlolarlan species discussed in the Figure 15. Proposed radlolarlan and planktonic foramlnlferal zones and correlation with previous work. References are as follows: (l) Antarctic area = Hays and Opdyke, 1967; Bandy and others, 1971. (2) North Pacific = Hays, 1970. (3) Tropics = Riedel and Sanfllippo, 1970, 1971. (4) Antarctic-subantarctic = Eennett, 1969, 1970. (5) New Zealand = Jenkins, 1971. (6) Tropics = Blow, 1969. Correlation of numbers 3, 5, and 6 with the magnetic scale Inferred from the present work; 4 was indirectly correlated with the scale by Kennett, and 1 and 2 are results of direct correlations. 96 PROPOSED ZONES (ANTARCTIC-SUBANTARCTIC) RADIOLARIA FORAMINIFERA PREVIOUS ZONES RADIOLARIA FORAMINIFERA 1 2 3 n g c E.TUMI- DULUM ZONE ¥ i S g X M ATUYA- MAI ZONE ui ' 3 * 1 c o ui 0 I- (EUJ U J o z P . PRIS MATIUI ZONE a,b X 0 .0 . O n -1 c c c /> T c UNZONED (S. PERE GRINA) S. PENTA ZONE d i/WW\AA < z a b >EREGRI Z O N E T (/) 0. PENUL TIMUS ZONE N.Z. co LU O 2 C O UNZONED -069- S. UNIVERSUS PARTIAL-RANGE ZONE 1 .79- < — -2.43 C. BICORNIS P.-R. ZONE S. PEREGRINA- L. HETEROPO- ROS CONCUR.-RANGE ZONE C O o S. PEREGRINA P.-R. ZONE -5.0 - S. DELMONTENSE ZONE G . TRUNC. 23 G.TRUNCATU- LINOIDES P-R. ZONE (SUBDIV. * NON EVOLUTION ARY) G. INFLATA ZONE G . PUNCTI- CULATA ZONE WVWWVW < U.° Z n o G.M. CONOIDEA- TRUNCAT ZONE G.MIOZEA CONOIDEA P.-R. ZONE E< UjUJ o-2z C050 o ' 20 19 OPOI- TIAN 18 G. MIOZEA MIOZEA ZONE ? ? ? < UJ h ' Q. 3 < <r 1 > < z o < 5? 98 preceding section. The zonal boundaries are defined by evolutionary datum planes (Table 3* Fig. 13). This zona- tlon has an advantage over earlier systems (Hays, 1965; Bandy and others, 1971) In that, Instead of combining ranges of regionally restricted species, four of Its nominate taxa are cosmopolitan species which have similar ranges In other climatic regions. Thus, correlations with equivalent zonations in other areas are feasible. Stlchocorvs delmontense Zone Paleomagnetlc age: ? - 5.0 m.y. (? - top of Epoch 5). Base left undefined; top given by the S. peregrlna datum plane. Zone characterized by the range of S. delmontense up to the first appearance of Its Im mediate descendant, S. pere grlna. This zone Is obviously a first approximation; its base cannot be defined presently because of the lack of older radlolarlans from high southern latitudes. Stlchocorys peregrlna Partlal-range Zone Paleomagnetlc age: 5*0-4.2 m.y. (lower-middle Gilbert). Definition: Base defined by the S. pere grlna datum plane (top of previous zone); top defined by the Lamprocyclas heteroporos datum plane. Zone character ized by the range of S. pere grlna up to the first appearance of L. heteroporos. subsequent Definition: Remarks: 99 to the latter species' evolu tion from Calocvclas marga- tensls. Remarks: The base of the zone, the S. peregrlna datum (Table 3)» also serves as a base for the tropical late Miocene S. peregrlna Zone (Riedel and Sanfllippo, 1971)* Consequently, both zones com mence at about 5*0 m.y.b.p. (Pig. 15). Stlchocorvs peregrlna-Lamprocyclas heteroporos Concurrent- range Zone Paleomagnetlc age: 4.2-2.5 m.y. (middle Gilbert- upper Gauss). Definition: Base defined by the L. hetero- poros datum plane (top of previous zone); top defined by the S. peregrlna extinction datum plane. Zone character ized by the concurrent ranges of the nominate species. Remarks: The S. peregrlna extinction datum in the upper Gauss is recognizable in many latitudes, as discussed before. This datum co-defines the top of the tropical Snongaster pentas Zone (Riedel and Sanfllippo, 1970) and, consequently, the base of the subsequent tropical Ptero- canlum prlsmatlum Zone. It follows that the top of the presently proposed zone cor relates with the S. pentas/P. prlsmatlum boundary, and that the latter limit falls within the upper Gauss (Pig. 15). Within the present zone several other species disappear (Table 3) but the nature of these events needs clarification. As dis cussed previously, the upper 100 limit of L. heteroporos Is not a reliable planktonic event in the area under study; it is probably migratory. Clathrocvclas blcornls Partial-range Zone Paleomagnetlc age: 2.5-1.8 m.y. (upper Gauss- middle Matuyama). Definition: Base defined by the S. pere grlna extinction datum (top of previous zone); top de fined by the Clathrocyclas bl- cornls extinction datum. Zone characterized by the range of the nominate species above the extinction of S. pere grlna. Remarks: Hays' (1971) data concerning the extinction of the nominate species, and the character istic morphology of typical specimens (PI. 1, fig. 5) make this zone particularly useful. Pterocanlum prls matlum. the nominate species of the tropical P. prlsmatlum Zone, also becomes extinct at 1.8 m.y.b.p. (Hays and others, 1969). Thus, both zonal boundaries are synchronous and both indicate the Pllocene- Pleistocene boundary (Fig. 15). The present zone contains the youngest sediments normally found in the present area. PesmoBpyrlB sponglosa dies out (top of Gauss; Hays, 1971) within it, but the form could not be recognized with certain ty above lowest Gauss in the present material despite its abundance and characteristic morphology in Gilbert sedi ments (Fig. 14E; PI. 1, fig. 5). Helotholus vema was 101 not Identified; It, too, be comes extinct during this Interval (Hays, 1971). The ? roblem with E. calvertense. ocally extinct since the base of the Gilsa event (Hays, 1971 ) ■ was considered earlier. Stvlatractus universus Partial-range Zone Paleomagnetlc age: 1.8-0.4 m.y. (middle Matuyama- mlddle Brunhes). Definition: Base defined by the C. bl- cornls extinction datumTtop of previous zone); top de fined by the S. universus ex tinction datum. Zone char acterized by the range of the nominate species subsequent to to the extinction of C. bl- cornls at the Pllocene- Pleistocene boundary. Remarks: The extinction of S* unlversus has been documented In a number of publications to have occurred at about 0.4 m.y.b.p. In high and low latitudes (Hays, 1965, 1970, 1971; Hays and others, 1969). The top of the present zone Is correla tive with the top of the synonymic zone of Hays' (1970) North Pacific zonatlon. The zone Is not represented In the present cores, since Matuyama age sediments are almost en tirely absent In them. No evolutionary events occurred during the last 0.4 m.y.; negative evidence alone Identifies this part of the Brunhes Epoch. Sediments of this time are best character ized by Snongonlegma antaretlea assemblages lacking S. unlversus. This Informal zone Is equivalent to Hays' 102 (1965) Omega zone (Table 2, Fig. 15). The proposed zonatlon will no doubt be refined as further evolutionary events become apparent. It Is im perative, however, that, If possible, planktonic events transcending local climatic regions are chosen to facilitate correlations. Ranges of Selected Planktonic Foraminlfera Blair (1965) first attempted to establish a plank tonic foramlnlferal zonatlon in antarctic-subantarctic areas based on material from the Brake Passage and the southern Pacific. Although chiefly a study of surface distributions, his work also gave evidence of climatic variations In three long cores. Subsequently, Kennett (1969b, 1970) proposed three foramlnlferal zones (Table 2, Fig. 15) for the period t = 0-1.2 m.y.b.p. He in directly assigned paleomagnetlc ages to the zonal 230 boundaries, and a 0.3-m.y. lsochron, based on Th dates (Geltzenauer, 1969)* served as age control in the upper sections of many of his cores. Since then several papers, based on or influenced by Kennett's work, have appeared (for example, see Jendrzejewsky and Zarillo, 1971; Kennett and Huddlestun, 1971; Watkins and Kennett, 1971* 1972). After the radlolarlan and magnetic stratigraphies of the cores were found to agree with previous work (Hays 103 and Opdyke, 1967; Bandy and others, 1971), analysis of the foramlnlferal ranges Immediately Indicated that lndis- crlmlnant application of Kennett's (1970) zones would re sult In different correlations (compare Figs. 13, 13). The cores dated as Gilbert-Gauss would be upper Matuyama- Brunhes If Kennett's system were followed strictly. And, even though the foramlnlferal assemblages resemble those of Kennett's study of 1970, there were significant dif ferences in species composition and ranges. A new zona tlon, agreeable with the actual paleomagnetlc ages and the radlolarlan zones, was needed. Just as in the radlolarlan section, the most Important foramlnlferal species and their ranges will be reviewed before proposing the zones. There is a marked difference between the foraminl- feral assemblages in £39-76, the northernmost core, and those in the other, southern cores. The former (c&. 36° S) latitudlnally corresponds to the North Central Fauna of Kustanowich's (1963) classification. Periodical intrusions of even warmer elements, however (such as Candelna nltlda and Globorotalla tumlda), gives it a transitional character between North Central and Northern Fauna in Kustanowich's system. The remaining cores contain Kustanowich*s South Central Fauna (essentially subantarctlc to antarctic), which is similar in composition to modern high-latitude assemblages described by several previous authors (Kustano wich, 1963; Boltovskoy, 1966, 1969; Kennett, 1969a), but In 104 addition contains several species now extinct. The dis cussion of the most significant species, therefore, centers around two groups: (1) those present In the entire area under study, and (2) those confined to E39-76. Table 3 lists all foramlnlferal datum planes and approximate paleo magnetlc ages. Figures 14A-H shows the ranges of the species In most paleomagnetically dated cores (see also Fig. 16). Plates 2-5 illustrate selected species and sub species, and Table 4 gives brief references to all fora- minifers. The following Indices are found throughout the entire area: 1. Globorotalla mlozea mlozea (sensu Walters, 1965; Jenkins, 1971). In New Zealand this form ranges from lower to upper Miocene (Walters, 1965) and typical specimens (PI. 2, figs. 1-3) abound In middle Miocene sediments of core E39-67, below a dlsconformlty at about 570 cm. Isolated, less typical Individuals (PI. 2, figs. 4, 5) are found in the Gilbert Mb" of E39-48, 56, and 67 (Figs. 14b, E, F). They represent the last occur rence of the subspecies and they may be equivalent to the Tongapurutuan (New Zealand upper Miocene Stage) specimens of Walters (1965). This level is designated the G. mlozea mlozea extinction datum and It has a paleomagnetlc age of 4.1 m.y. (Table 3)« Olsson and Goll (1970) and Olsson (1971), In North Pacific DSDP material, found G. mlozea s.l. disappearing in the bottom of their faunal unit VI, 105 indirectly correlated with a level between Gilbert "b" and "a" (Pig. 13). This is remarkably close to the present finding. G. mlozea is also useful for correlations in Miocene strata of the North Atlantic (Berggren, 1971). Thus, it serves for correlations of cold to temperate areas in both hemispheres. A restudy of the Gllbert-Gauss tropical Indian Ocean core V20-163 Indicates (Bandy, pers. comm.) that the G. mlozea lineage even Invaded tropical areas at certain periods. Consequently, for the first time, indices are available that can help to bridge the gap between the Mlocene-Fliocene Neogene zones of the tropics (Blow, 1969) and temperate or cold water equiva lents . 2. G. mlozea conoldea ranges in New Zealand, where it was originally described (Walters, 1965), from middle Miocene (Lillburnian Stage) to the very basal part of the Pliocene (basal Opoltian Stage; Jenkins, 1971). In the cores it is present in the oldest Gilbert sections re covered. Its upper limit is associated with the upper Gauss, above the Kaena event (Fig. 13). This level is arbitrarily placed at 2.6 m.y.b.p. (Table 3) in view of the uncertainties in interpreting sedimentation rates and magnetic stratigraphy in cores that contain the G. mlozea conoldea extinction datum. It is Just below the P. tltan- L. grande extinction datum mentioned in the radlolarlan section. The present subspecies is also found in the North 106 Pacific (Olsson and Goll, 1970; Olsson, 1971), the North Atlantic (Berggren, 1971; Vincent, pers. comm.) and In the tropical Indian Ocean (Bandy, pers. comm.) with ranges comparable to those found in the present cores. The morphology of this form varies from typical (c£. Walters, 1965; Jenkins, 1971 and PI. 2, figs. 6-9) to forms with higher arched apertures that show affinities to G. punctlculata punctloulata. 3. G. mlozea spherlcomlozea. The range in New Zealand of this rounded and compact subspecies is very short, comprising only the Kapitean and the base of the Opoltian Stages (Jenkins, 1971)* As with its predeoessor, it is also in the earliest Gilbert material available here, and its upper limit coincides with the G. mlozea conoldea extinction datum in the upper Gauss (Pig. 13. Table 3)* This age agrees with its extinction in New Zealand (Jenkins, 1971), where both forms have identical upper limits. See Plate 2 for illustrations. Both subspecies of G. mlozea should probably be considered to be distinct species, despite some transi tions among younger specimens. It is unlikely that sympatric subspecies, which presumably occupied one partitioned niche and similar habitats, could preserve their genetic independence for the duration of their con current ranges. More reasonably, speciation occurred dur ing the Kapitean Stage, impeding further genetic exchange. 107 The writer agrees with Jenkins' (1971) contention that the G. crassaformls hloserles described by Kennett (1966) In upper Miocene to Pliocene strata of Hew Zealand In reality corresponds to parts of the G. mlozea £.1. lineage Mclnnes (1965) and Walters (1965) found earlier In equivalent sections. Virtually all of Kennett's figures (1966) of G. crassaformls actually Illustrate G. mlozea spherlcomlozea. Olsson and Goll (1970) found G. mlozea spherlcomlo zea In their North Pacific faunal units V and VI, which they correlate with middle Gilbert-lower Gauss by extra polation. This, again, agrees with the present results (Pig. 13), but the upper limit of the form in their material Is considerably below that of G. mlozea conoldea. Thus, the extinction level of G. mlozea spherlcomlozea cannot be employed outside the New Zealand-Australian area with confidence. Only a regional datum plane Is therefore based on it (Table 3; Pig. 13)• It should be added that both Colalongo (1970) and Sprovlerl (1971) have found a form similar (If not identical) to G. mlozea spherlcomolzea (G. mlozea sanhoae) In Tortonlan and lower Messlnlan sections of Sicily. The fauna of Messlnlan age found just above the Tortonlan In the section at Marche studied by Colalongo Is essentially the same as that of the Messlnlan neostratotype at Pasquasia-Capodarso (Colalongo, 1970). It is, therefore, correlative with Neogene Zone 18 (Bandy, 108 1971). A. G. punctlculata punctlculata. This large foraminifer (PI. 2, figs. 16-18) apparently does not occur in the New Zealand sections, yet It is common in uppermost Miocene to Pliocene strata of the Mediterranean region (for example, Colalongo, 1970), the Pliocene- Pleistocene of the North Atlantic (Berggren, 1971b), the experimental Mohole off Baja California (Bandy, 1971)* the Pliocene of the North Pacific (Olsson and Goll, 1970; Olsson, 1971), presumably reworked Pliocene sediments of the Brake Passage (Herb, 1968), and in allegedly Pleisto cene sediments of the subantarctlc Pacific (Kennett, 1970). Its initial appearance cannot be traced in the material under study; it occurs concurrently with the above sub species in the oldest Gilbert samples available, but it is absent in the middle Miocene section of core E39-67. In the North Pacific (Olsson and Goll, 1970) it first appears at the base of faunal unit V, which in directly correlates with upper Gilbert, above event "a". This is above the earliest speolmens in the present material (Pig. 13). Considering, however, that Olsson and Goll's correlation with the polarity scale is indirect, the discrepancy seems negligible. Blow (1969) thought that this form developed from G. subscltula during the later part of Zone N. 19, or earliest N. 20. This appears chronologically impossible because G. punctlculata 109 £.g. Is already present in the top of the Messlnlan (Neo- stratotype, Pasquasla-Capodarso, Italy; Colalongo, 1970), which correlates with Zone N18 (Blow, 1969; Bandy, 1971)* In addition, morphologically a certain gradation exists between G. mlozea conoldea and G. punctlculata s,.£. that suggests a possible lineage homologous to the evolution from G. mlozea spherlcomlozea to G. BUB9&lg^la$a BMaa& (see below). Such an interpretation Is concordant with the timing of the initial appearances. The upper limit of G. punctlculata £.£., in the material under study, again falls within the upper Gauss, just before the G. mlozea conoldea-spherlcomlozea extinction datum (Pig. 13, Table 3). Its absence at higher levels is possibly due to emigration; it persists in other temperate areas into at least Zone N22 to basal N23 (Bandy and others, 1971)* Reports of G. punotlculata s.s. in Holocene sediments (Banner and Blow, I960; Blow, 1969) are not convincing and may result from the analysis of reworked specimens, or from misidentlflcations. Upon close examination, most Holocene records can be referred to varieties of G. crassa- formls (e.g., Kustanowich, 1963) or to G. punctlculata padana. 5. G. punctlculata padana (PI. 2, figs. 13-15)» originally described from the lower to middle Pliocene of Italy (Dondl and Papettl, 1968), now has been found also in the top of the Messlnlan neostratotype (Colalongo, 110 1970). Many authors, especially In New Zealand, have con sidered this form to be a variant of G. Inflata, from which It differs primarily by the flat, "crassaformis- like" dorsal side. It Is unquestionably related to both G. nunctlculata nunctlculata and £.. mlozea snherlcomlozea and probably closer to the latter than to the former, des pite the Implications conveyed by the nomenclature. Mclnnes (1965) has described some of the transitional variations encountered In the evolution from G. mlozea &.I. to G. mlozea snherlcomlozea and finally to G. nunctlculata nadana (=G. lnflata of New Zealand authors) occurring In the upper Miocene-lower Pliocene of New Zealand. Com parable variants are also found in the present Gilbert- Gauss cores. It is Impossible, however, to define one level where G. nunctlculata nadana commences to dif ferentiate. It seems plausible that the evolution of this form took longer In this area than In New Zealand. In terms of abundance, G. mlozea snherlcomlozea Is dominant in Gilbert sediments and G. nunctlculata nadana in the Gauss, but transitional specimens are common in Gilbert to lower Gauss. One of the Opoitian (New Zealand Pliocene) speci mens Kennett (1966) Illustrated (££.. clt.. PI. 1, Pigs. 3a-b) as G. crassaformls is presently interpreted as G. nunctlculata nadana. Ihis extends Jenkins' (1971) argu ment that Kennett actually described a partial G. mlozea Ill lineage rather than a G. oraseaformls bioserles and that G. nunctlculata padana should be Included as the end member of Kennett's (1966) hypothetical lineage. 6. G. lnflata Inflata. The first appearance of this widely known temperate foramlnlfer Is clearly depen dent of latitude (Fig. 13* Table 3). In the northernmost core containing Gilbert sediments (£39-67)* It is--although rare— present Just below Gilbert "b" (Fig. 14B). To the south (core £39-48* ca. 46° S) the first specimens appear Just above Gilbert "b", and It becomes abundant during Gilbert "a” (Fig. 14F). In the southernmost core (E39-40, 52° S) G. lnflata &.s. first appears during the early Gauss (Fig. 14G). There Is considerable controversy about the Initial appearance and origin of this species on a world-wide basis (Banner and Blow, 1967; Blow, 1969; Yen, 1971) and many mlsldentlflcatlons are evident. The present finding of G. lnflata (sensu strlcto. see Banner and Blow, 1967; Blow, 1969; and PI. 2, figs. 19 of present study) In sediments at least as old as Gilbert "b" means that It evolved from an as yet unknown ancestor prior to this time. This supports Blow's (1969) statement that G. 1&- flata s.s. occurs In Zone N18, If not N17. Moreover, un less a polyphyletlc origin Is called upon to explain It, the supposed evolution of G. lnflata from G. bononlensls- G. punctlculata In the late Pliocene of Italy (Zone £21?) 112 suggested by Lamb and Beard (1972) is refuted. The forms identified In Miocene-Pliocene sections of New Zealand (Mclnnes, 1965; Jenkins, 1971) are inter preted here as G. nunctlculata nadana (see above); G. ln flata s.s. is apparently not found in these sections. Con versely, in the present material it is probably the most common species, in part because of the latitude of most cores (G. bulloldes and G. lnflata are dominant components of Holocene assemblages In the area; Kustanowich, 1963). Also, because of its resistance to solution, at times it is the only species remaining in the samples. G. lnflata s.s. varies morphologically and normally is found in three basic shapes that may have four types of wall structure. Yen (1971) has typified these variants by statistical analysis. 7. G. crassaformls s,.l. At least three basic variants (perhaps subspecies) of this foraminifer con sistently occur in the northern cores (E39-67t E39-76). Although similar, none correspond exactly to Blow's (1969) subspecies, mainly because of generally sharper peri pheries and a tendency towards development of a keel in most specimens. Figures 20-24 (PI. 2) and 1-3 (PI. 3) show representative examples of each basic variation. It should be noted that transitions also exist, rendering it a difficult group to study. The variety of a less conical ventral side, with sharp peripheric margins (PI. 3* 113 figs. 2-3), is sometimes found In other cores. Parker (1967)» Bolli (1970), and especially Ujiie and Miura (1971) have Illustrated comparable specimens from tropical areas. Lamb and Beard (1972) hypothesized a Pliocene to Holocene lineage that, judging from their illustrations, also involves this group. The G. crassaformls variants lacked a defined range; most were rare and intermittently distributed throughout Gilbert, Gauss, and Brunhes sedi ments (Figs. 14A-D). Interestingly, none was identical to the specimens illustrated as G. crassaformls by Kennett (1970) and Blair (1965) from southern Pacific cores. In fact, the latter do not even fit the species' normally ac cepted morphology and some (Kennett, 1970, Fig. 2, nos. 9-11) are comparable to G. £f. crassula viola discussed later. Moreover, the present writer believes that the G. crassaformls bioseries which was described by Kennett (1966) from upper Miocene-Pliocene samples of New Zealand is actually a different branch of the G. mlozea s.l. line age. The fact that none of his specimens of G. crassa- formls compare with the present specimens tends to support this conclusion. Olsson (1971) found G. crassaformls initially appearing at the Gilbert-Gauss boundary in North Pacific DSDP cores by indirect correlation with the paleo- magnetic scale. The lack of illustrations unfortunately impedes adequate comparisons. 8. G. truncatullnoldes (PI. 3» figs. 6-11) will 114 be discussed later In detail due to Its Importance as a guide fossil and its striking range in the present cores. It is a common species in the entire area, at times con stituting over 10 percent of the fauna. Its initial ap pearance in the lower Gauss (Fig. 13) represents the G. truncatullnoldes datum plane (Table 3) of regional character. Its paleomagnetlc age varies from 3*3 to about 3.0 m.y. Both of Blow's (1969) hypothetical subspecies can be found, but their value as such seems questionable. It is difficult for the present writer to visualize how two subspecies which are probably sympatric could maintain separate gene pools without the action of some barrier. According to Blow (1969) both forms are seen together in samples from a variety of latitudes, climates, and depths. He places special emphasis on their similarity of habitats and, presumably, Identical niche. If these are subspecies in a biological sense, some temporal, spatial, or ecologlc differentiation of populations should be encountered, at least somewhere, which would indicate some sort of barrier. And, transitional specimens, accumulating after death in sediments, should live where (when) populations overlap. These theoretical requirements should be considered when subspecies are established, especially among Holocene spec ies where evaluation of these considerations is simpler than in fossils. 9. G. cf. crassula viola. In several northern 115 cores (Figs. 14A-D) specimens were found occasionally that show affinities to this tazon (PI. 3, figs. 4-5). Their range cannot be exactly defined due to their scarcity, but they are chiefly Gilbert to lower Gauss forms. Al though they do generally resemble both G. crassula cono mlozea and G. crassula viola, they are generally less conical than the typical G. crassula conomlozea and have an elongate, slit-like apperture, but they also lack the strongly llmbate dorsal sutures of typical G. crassula viola. Conversely, their chambers are less embracing than those of the former. The writer agrees with Blow (1969) in considering Kennett's (1966) G. conomlozea subspecific to G. crassula. The present forms might represent transi tional morphologies that are to be expected whenever (wherever) subspecific populations overlap genetically. G. aemlllana and G. crassacrotonensls probably are also expressions of this same G. crassula plexus. Some of Kennett*s (1970, Fig. 1, nos. 9-11) and possibly Blair's (1965, PI. 1, Fig. 7) G. crassaformls may also belong to this general group. Colalongo (1970) encountered G. crassula conomlozea in the lower part of the Messinian neostratotype (Pasqua- sia-Capodarso). The illustrations are not explicit enough to allow detailed comparisons, but they resemble some of Kennett's (1966) drawings. The following foraminlferal Indices were restricted 116 to E39-76 (Pig. 14A) (oldest to youngest appearance): 1. Pullenlatlna prlmalls (PI. 3» figs. 15-16). This species occurred throughout most of core £39-76. Usually abundant because of selective solution, It becomes increasingly difficult to differentiate from P. obliaullo- culata s.b. in younger horizons. It changes colling direction abruptly, from left below to right above, at about 800 cm (above the Mammoth event; Fig. 14A). In equatorial cores, Hays and others (1969) have recorded this well-known colling shift In the upper Gilbert, above event "a" (see also Bandy, 1963; Bandy and Wade, 1967; Bolli, 1966; Bronnlmann and Resig, 1971; Lamb and Beard, 1972). This casts doubt on the reliability of this coil ing datum for precise correlations since a timing dif ference of nearly 1.0 m.y. is involved. In the Kurotakl Formation of the Japanese Boso Peninsula, a similar switch occurs (Takayama, 1967). If the paleomagnetic stratigraphy of this section (Nakagawa and others, 1969) is interpreted so that the formation correlates with the Mammoth event (Bandy and others, 1971; see details in discussion of G. truncatullnoldes datum), evidence from northern marginal areas would also question the synchroneity of this colling switch. Interestingly, the Kurotakl formation and the present cores were deposited in comparable climatic regions at the margins of Pullenlatlna's distributional range. Both P. prlmalls and P. obllqulloculata (discussed 117 below) are absent from upper Miocene-Pliocene New Zealand sections (Jenkins, 1971). P. obllaulloculata Is, however, a member of the Holocene North Central Fauna (Kustanowich, 1963) that surrounds the northern tip of that country and comprises the location of £39-76. 2. Sphaeroldlnella dehlscens lmmatura (PI. 3, figs. 19-22) and S. dehlscens dehlscens (PI. 3» fig. 23). In contrast to Blow (1969), S. dehlscens lmmatura Is here considered to be a valid chronological subspecies in view of the clear transition from these primitive populations, usually associated with Zone N19 (Parker, 1967; Blow, 1969; Bandy and others, 1971; Bronnimann and Reslg, 1971), to the advanced S. dehlscens dehlscens of later zones. The transition is hard to define exactly in time, since it is a matter of subjective decisions (Bronnimann and Reslg, 1971) but, by the latter part of N19, S. dehlscens dehlsoene has definitely acquired Its characteristic apertures. This can also be seen In the present core, although fully modern specimens are rare, most likely due to solution. Since S. dehlscens lmmatura has such a greatly restricted surface compared to the nominate subspecies, It is logical that solution would affect it to a lesser degree. Consequently, throughout the lower part of £39-76, it is the dominant form (Fig. 14A). At about 340 cm most specimens no longer possess the characteristic minute dorsal aperture and should be considered as S. dehlscens dehlscens thereafter. 118 In the absence of G. altlsnlra altlsnlra. S. dehlscens lm matura seems valuable as another means of defining Blow's Zone N19 (Bronnlman and Reslg, 1971). Bandy and others (1972) have Bhown that In mid latitudes there Is a gradual change from primitive S. dehlscens (= S. dehlscens lmmatura of present study) to more typical forms (= S. dehlscens dehlscens) at a level above the Mammoth event, near the extinction of Snhaerol- dlnella subdehlscens. Globorotalla pleslotumlda and g. merotumlda. Similarly, in V20-163 (tropical Indian Ocean), Sphaeroldlnellopsis bpp. completely dominate assemblages until about the base of the Gauss. At this level Sphaerol- dlnella dehlscens commences to increase in abundance, cul minating In complete dominance of this species just above the Mammoth event. 3. Pullenlatlna obllqulloculata obllaulloculata. The first typical specimens (PI. 3, fig. 17) appeared at 790 cm (£39-76), but a few questionable individuals were also seen at 850 cm (Fig. 15A). If this can be taken as the initial appearance, a risky assumption in view of the severe solution and the marginal location of the core with respect to the species' areal of distribution, excellent agreement with Hays and others' (1969) data is reached. They showed that it initially appears in the middle Gauss, just above the Mammoth event, which is essentially identi cal to the present situation (Fig. 13). This lends addi 119 tional support to the correlation of Zone N19 (or parts thereof) with parts of this core and, consequently, with at least parts of the Gauss Epoch (Bandy and others, 1971; Fig. 15 of present study). 4. Globorotalla lnflata trlaneula. n. subsn. This subspecies (PI. 5) Is described and discussed under Taxo nomic Botes. It Is a characteristic component of the lower part of E39-76 (middle to upper Gauss; Fig. 14A), but does not occur In the short Matuyama and Brunhes sections of the core. It Is the same form which Lamb and Beard (1972, PI. 27, Figs. 1, 2, 5) called G. lnflata (variant) in material from the early Pleistocene of the Gulf Coast. Its general range, therefore, may be longer than in the present core. 5. £. tosaensls (PI. 3, figs. 12-14). Both of Blow's (1969) controversial subspecies are represented In E39-76, although they were rare and intermittent (Fig. 14A). As pointed out in the discussion of G. truncatull- nold.es, it is difficult to visualize how these forms can be assigned to subspecific levels; here they are interpret ed as morphological variants. Hays and others (1969) have demonstrated that the form initially appeared in the middle Gauss of Equatorial Pacific cores. Olsson (1971) found it in what he in directly correlated with upper Gauss of North Pacific DSDP drillings. Both findings are in accord with the range in 120 this study (Fig. 13). Further details follow In the section on the G. truncatullnoldes datum. 6. Pullenlatlna obllqulloculata flnalls (PI. 3, fig. 18). Typical representatives occurred rarely and scattered In the upper 115 cm of E39-76. This part of the core Is Interpreted as Brunhes and uppermost Matuyama since obllqulloculata flnalls was found to be restricted to these ages by Hays and others (1969) and Ujlle and Mlura (1971). The Globorotalia truncatullnoldes Datum Plane In the Present Area The first appearance of G. truncatullnoldes was, in the past, one of the most reliable planktonlc foramini- feral datum-planes of the Neogene. Widely accepted as marking the beginning of the Pleistocene at about 1.8 m.y.b.p. during the Matuyama Epoch (Berggren, 1968), this datum must now be restricted to areas north of about 36° S In the southern hemisphere (Theyer, 1972). In the present region Its range begins in the lower Gauss, at the base of, during, or lust above the Mammoth event in the cores that were paleomagnetically dated (Figs. 13, 14A-D, F, G, 16). This predates Its first occurrence in lower latitudes by about 1.3 m.y. In addition to the paleomagnetic evidence, G. truncatullnoldes overlaps the following upper Miocene to Pliocene radlolarlans and foraminifers In both dated and 121 undated cores: Clathrocyclas blcornla. Eucyrtldlum calvertense, Lamprocyclae heteroporos. Prunopyle titan, Stlchocorys peregrlna. Globorotalla mlozea conoldea. G. mlozea spherlcomlozea. Pullenlatlna prlmalls. and Snhaerol- dlnella dehlscens lmmatura (Pigs. 13, 14A-D, F-H, 16). It Is Important to note that G. tosaensls. the supposed ancestor of £.. truncatullnoldes (Banner and Blow, 1965; Berggren, 1968; Blow, 1969), occurs In different morpholo gies and at different levels In E39-76. In the lowest part, partially preceding and overlapping the first G. trunca tullnoldes (Pig. 14A), rare specimens are found that show no indication of a keel, or a keel only on the last chamber (PI. 3, figs. 12-13; PI. 4). They correspond to the "tenuitheca" morphotype (Blow, 1969), and are here interpreted, respectively, as G. tosaensls and primitive G. truncatullnoldes. Higher in the core G. tosensls re appears, but they seem to correspond to Blow's (1969) "pachytheca" morphology (= G. tosaensls pachytheca. sensu Blow, 1969; PI. 3, fig. 14 of present paper). Neither form of G. tosaensls was found in the other cores, suggest ing that it does not live south of approximately 45° S. It is very difficult to reconcile Berggren1s (1968) findings with the present cores. If G. truncatullnoldes and G. tosaensls are both valid species, then it must be assumed that an Identical evolutionary change took place at different times and in separate hemispheres. In a strict 122 sense, modern G. truncatullnoldes should then he considered composed of two entitles. The other Immediate solution would be to Interpret G. truncatullnoldes and G. tosaensls as subspecific groups, or perhaps even lower, ecological variants. Since both first appear at Identical times (base of the Mammoth, see later), one In temperate (G. tosaensls) and the other In subantarctlc areas (G. truncatullnoldes). It might be speculated that an environmentally controlled relationship did exist between them. Whatever the true connection, a direct speclatlon from one to the other at the Pliocene-Pleistocene boundary (Berggren, 1968) Is now questionable. G. truncatullnoldes was already fully developed about 1.3 m.y. before the onset of the Pleisto cene. Kennett and Geitzenauer (1969) were correct in ex pressing doubts regarding the supposed simplicity of this speclatlon. Previous studies that supported a Pliocene appear ance of G. truncatullnoldes (Aokl, 1963; Ingle, 1967; Jenkins, 1967, 1970, 1971; Takayama, 1967; Beard, 1969; Bandy and Ingle, 1970) have generally been disregarded in the past, or were the result of misidentlficatlons. Es pecially relevant among the former group is the report of definite G. truncatullnoldes with G. tosaensls in the Kurotakl Formation (basal Pliocene) of the Boso Peninsula, Japan (Aokl, 1963, and pers. comm, to 0. L Bandy; Taka yama, 1967)* Paleomagnetlc analysis of late Cenozoic Boso 123 Peninsula sections (Nakagawa and others, 1969) allows a tentative correlation of the Kurotakl Formation with the Mammoth event (Bandy and others, 1971)» which agrees with results of the present study. Moreover, the report of alternating populations of G. truncatullnoldes and G. tosaensls at and below the Pliocene-Pleistocene boundary In a South Pacific core (Kennett and Geltzenauer, 1969) also points to a pre-Pleistocene existence of G. trunca tullnoldes. It Is noteworthy that the combined range of the G. tosaensls-G. truncatullnoldes complex Is identical In the tropics and in the present area. Hays and others (1969) have shown that S.. tosaensls commences to appear at the base of the Mammoth event (V20-l63)» which is remark ably similar to the initial appearance of G. truncatull noldes in most of the cores under study. It Is also In accord with the appearance of G. tosaensls in E39-76 (Fig. 14a) . It must be conceded that a marginal chance exists for the abundant G. truncatullnoldes to be contaminants, especially since mixing is noticeable In the tops of many cores. The number of cores involved, the agreement of radiolarian, foraminlferal, and paleomagnetic evidence, In addition to the widely separated locations, however, make this a very unlikely hypothesis. Planktonlc Foramlnlferal Zones In contrast to the many evolutionary events that define the radlolarlan zones proposed earlier, few phylo- genetio changes (Table 3) can be drawn upon to establish planktonic foramlniferal zones In the late Neogene of these latitudes. It must be reiterated that the zonatlon to be pro posed, and the radlolarlan zonatlon established earlier, are primarily Intended to facilitate correlation from areas essentially south of 45° S with existing models for lower latitudes. Consequently, climatically controlled sub divisions, which are usually of very restricted applica tion, were avoided. The advantage of this Is illustrated by E39-76; three of the proposed zones can be recognized In It and, in turn, it can be compared with tropical Neo gene zones. Four zones, based on partial and concurrent ranges of three species and the resulting datum planes, can be proposed (Figs. 13, 15; Table 3): Globorotalla mlozea mlozea Zone Paleomagnetlc age: ?-4.2 m.y. (?-middle Gilbert) Definition: Base undefined; top defined by the G. mlozea mlozea extinction datum. Zone characterized by the range of the nominate taxon. Remarks: The zone is preliminary in that further Miocene material is needed from high latitudes for a definition or its base. Globorotalla mlozea conoldea Partlal-range Zone Paleomagnetic age: 4.2-3.3 m.y. (middle Gilbert- lower Gauss). Definition: Base defined by the G. mlozea mlozea extinction datum (top of previous zone), top defined by the regional G. truncatullnoldes datum plane. Zone characterized by the partial range of the nominate taxon subsequent to the extinction of G. mlozea mlozea up to the first appear ance of G. truncatullnoldes. Remarks: The G. truncatullnoldes datum plane has been reviewed earlier. The zone partially correlates with the G. mlozea snherlco mlozea Zone of the Upper Miocene of New Zealand (Jenkins, 1971) and, hence, with parts of the Kapitean Stage of New Zealand (Pig. 15). Globorotalla mlozea conoldea-G. truncatullnoldes Con- current-range Zone Paleomagnetic age: 3.3-2.6 m.y. (lowest-uppermost Gauss). Base defined by the G. trunca tullnoldes datum plane (top of previous zone); top defined by the G. mlozea conoldea extinc tion datum. Zone characterized by the concurrent ranges of the nominate taxa. This zone correlates at least partially with the Pliocene Opoltlan Stage of New Zealand (Jenkins, 1971; Pig. 15 of present study). Definition: Remarks: r i 126 Globorotalla truncatullnoldes Partial-range Zone Paleomagnetic age: 2.6-0.0 m.y. (uppermost Gauss- Brunhes). Definition: Base defined by the G. mlozea conoldea extinction datum. Zone characterized by the range of the nominate taxon subsequent to the extinction of G. mlozea conoldea. Remarks: The zone Is very long (at least 2.6 m.y.), but It can only be subdivided on the basis of climatically controlled events in the present latitudes. Any such subdivision will be severe ly Influenced by the latitude of the samples. Studies on latitudinally-restricted morpho- types of Globlgerlna bulloldes. a species that is very abundant in subantarctlc areas, are es pecially promising in this con text (Bandy, 1972). The S.. mlozea lineage will probably assume an im portant role in future zonations of high to mid-latitudes. Previously known only from New Zealand (Walters, 1965; Jenkins, 1971), this diverse group of subspecies occurs in upper Miocene to Pliocene DSDP material from the North Pacific (Olsson, 1971), in Miocene DSDP drillings of the North Atlantic (Berggren, 1971b), and in an upper Miocene to basal Pliocene core from the Gibraltar area (Vincent, pers. Comm.). Their ranges in all these areas generally agree with those presented here (Figs. 13, 14). Since these forms also invaded tropical areas, as shown in Gilbert-Gauss Indian Ocean core V20-163 (Bandy, pers. 127 comm.), potentially very useful Indices for correlations across different water-masses are suddenly at hand. A careful evaluation of the taxonomy and evolution of this lineage still needs to be done; one Immediate problem Is the presently suggested relationship between the G. nunctl- culata-group and this lineage. Unfortunately, the cores are not long enough for this task. A number of subantarctlc cores containing discon tinuous stratlgraphic sections ranging from early Eocene to late Miocene (Margolls and Kennett, 1971) have shown that many Index fossils from early and mid Cenozolc sections of New Zealand and elsewhere are common even at these latitudes. It Is hoped that the antarctic DSDP Legs will recover sufficient material to allow completion of a hlgh-latltude Cenozolc planktonlc zonatlon. Blostratlgraphlc Interpretation Pore E39-76 Due to Its location (Fig. 1, Table 1) at the southern boundary of subtropical planktonlc faunas, where summer surface Isotherms reach 20° C (Kustanowlch, 1963)» E39-76 shares Indices with the proposed zonatlon and tropical Neogene zones (Blow, 1969). Unfortunately, It lacks radlolarlans which Impedes corroboration from this group. And, solution Is extreme throughout the core (Figs. 8, 14a) accounting for the absence of most foramlnlfers at some levels. Where present, Indices Indicate that the £.• mlozea conoldea Zone Is confined to the last 40 cm of the core, If at all present. There were no G. truncatull noldes found here, but here solution Is especially severe and thus might be responsible for this absence. The G. mlozea conoldea-G. truncatullnoldes Zone comprises the rest of the core to 300 cm, where the G. truncatullnoldes Zone commences. At 250 cm a hiatus leads upwards Into a short Matuyama section followed by Brunhes. Only minor mixing of elements from these different ages occurs (Fig. 14A). The presence of Pullenlatlna obllQulloculata flnalls down to 230 cm, and also In one trigger core sample, corroborates these Interpretations. This pattern of a short Brunhes age top Is repeated In many other cores. Tropical Indices allow an Indirect correlation with Blow's (1969) Neogene zonatlon. If Snhaeroldlnella dehlscens lmmatura is confined to Zone N19 (Parker, 1967; Blow, 1969; Bandy and others, 1971; Bronnimann and Beslg, 1971)» and if P. obllqulloculata s.fi. first appeared In the lower to middle part of this zone (Blow, 1969; Bandy and others, 1971)» then the lower third of £39-76 (up to at least the disappearance of S. dehlscens lmmatura at about 320 cm) correlates with N19 (Fig. 15A). The con sistent presence of P. prlmalls and the increasing development of S. dehlscens dehlscens at higher levels in 129, the core, strengthen the correlation. Consequently, the upper half, if not most, of Zone N19 corresponds to the Gauss. The bottom of N19 is probably not far below the bottom of £39-76 (top of Mammoth event) as indicated by the scarcity of S. dehlscens &.I. in the lowest samples. Bandy and others (1971) arrived at strikingly similar re sults by reinterpreting Hays and others' (1969) and Parker's (1967) data. In addition, Glass and others (1967) also demonstrated that S. dehlscens first appeared at the Mammoth event. Since the base of N19, and consequently the top of N18, is one basis for defining the Miocene-Pliocene boundary (Parker, 1967; Bandy and others, 1971), accurate correlation of either zonal boundary with the magnetic polarity scale is of considerable importance. Core E39-67 Next in southerly progression, £39-67 again lacks radiolarians. Analysis of foramlniferal indices above the disconformity at 570 cm (Pig. 14B), however, permits clear recognition of the three oldest foramlniferal zones pro posed. The G. truncatullnoldes Zone is missing entirely. Hone of the warmer elements of £39-76 is found in this core so that direct comparison with Blow's (1969) zonatlon is ruled out. Below the disconformity, 430 cm of lower middle 130 Miocene sediments occur. On the basis of Praeorbulina glomerosa clrcularis. Orbul.lfift suturalis. Globorotalla mlozea mlozea. and Globlgerlna woodl woodl the sediments correlate with the Llllburnian Stage of the New Zealand Miocene (Jenkins, 1971). The absence of Globorotalla mayerl mayerl confines this material to the 0. suturalis Zone of this stage, or merely indicates that the G. mayerl mayerl Zone of New Zealand cannot be defined in this lati tude. There are other elements, however, which make this lower portion of the core seem suspicious. Specimens of G. woodl connects found in many samples indicate contamina tion with lower Miocene (Jenkins, 1971) and occasional Globlgerlna nepenthes gives it affinities with upper Miocene. In New Zealand the latter does, apparently, overlap most of the previous species in Llllburnian rocks (Jenkins, 1971)» so that its occurrence here may not be anomalous. On the other hand, G. glomerosa clrcularis and £.. suturalis correlate this core section with Zone N9* several zones below G. nepenthes1 range in Blow's (1969) scheme. If this core section represents most of the New Zealand Llllburnian Stage, then two reversed and two normal magnetic polarity sequences can be expected in future paleomagnetic studies of equivalent rocks (Fig. 14B). Ill Other Cores 131 In cores with known paleomagnetic stratigraphies (Table 1, Figs. 1, 11A-G) ranges of zonal markers and other planktonlc indices permit direct correlation of the proposed planktonlc zones with the magnetic scale (Figs. 14C-H, 16). The remaining, undated cores were correlated with the proposed planktonlc zones by analyzing ranges of zonal indices and thus could Indirectly be placed in the magnetic reference scale (Fig. 16). Clearly, the predominant zones represented in the cores are the S. nereerina-L. heteronoros radlolarlan Zone and the G. mlozea conoldea and £. mlozea conoldea-G. truncatullnoldes foramlniferal Zones, which paleomagnetl- cally represent mainly upper Gilbert to upper Gauss (Fig. 15). Exceptions are the youngest cores (E39-15* 22, 24, 42, 46), which instead are all restricted to the C. bl oom is radlolarlan Zone and the G. truncatullnoldes foramlniferal Zone of upper Gauss and younger ages. The oldest radlolarlan zone is found in E39-56 (Fig. 14E) and the oldest foramlniferal zone in E39-48 and 67 (Figs. 14B, F). Earlier, it was shown that Zone E19 of Slow's (1969) zonatlon can be correlated with most of the Gauss Epoch. Thus, despite the lack of Blow's nominate taxa, it can be argued that this zone, or better its cold-water equivalent, la most representative of the ages in the cores.___________ Figure 16. Biostratlgraphlc interpretation and generalised correlation of cores £39-14, 15, 20, 24, 42, 44, 50, and 51* Note graded turbidlte section of Gauss age within a seem ingly Matuyama portion of core 339-20. The Brunhes sections of cores £39-42 and 44 both contain E. calvertense which might be re worked. 132 3 9 -1 4 39-15 3 9 - 2 0 3 9 -2 4 3 9 - 2 7 3 9 - 4 2 3 9 - 4 4 3 9 - 5 0 39-51 0 2 - 4 - e> z Ui UJ t c o O 8 10 - 12 - U0. 0 2 I- w v > o o o OH bJ o MATUY. ? GAUSS ? M ID D LE G A U S S i GRADED TURBIDITE (GAUSS) CB * C. BICORNIS CM - C.MARYLANDICUS EC«E. CALVERTENSE LG*L GRANDE L H* L. HETER0P0R0S 0 0 « 0R0SCENA (DIGITATE) P T * P . TITAN SP * S. PEREGRINA G I * G. INFLATA GMC • G . MIOZEA C0N0IDEA GT > G . TRUNCATULINOIDES o . 5 * - x o o o (9 J u k i h io m O _JUI o M ATUY. - LATE GAUSSl u a x c l t e l 0- 1 0 ) I ■ u KSO oou o K - 2 U H O O o Id CL — a oQ (9 UJ o O • c K J % BRUNHES- BRUNHES-= EARLY GAUSS c . GAUSS t ■ NORMAL □ REVERSED Q HORIZONTAL GAUSS ? L A T E S T GAUSS G A U S S - G IL B E R T G A U S S - G IL B E R T 133 134 Comparison of Proposed Zones with Previous Work A comparison with previous work of the proposed zones and presently found ranges of indices shows agree ment in most aspects and discrepancies in a few Instances (Pigs. 13, 15). Among earlier foramlniferal work, Kennett's (1969b, 1970) zonatlon needs specific attention, since it is the only previous comprehensive zonatlon of higher southern latitudes. The ranges of G. lnflata. G. nunctlculata nunctlculata. G. truncatullnoldes. and G. crassaformls in this study contrast markedly with the present results (Fig. 13) and, moreover, partially disagree with findings from the North Pacific (Olsson and Goll, 1970). These discrepancies cannot be due to climatic factors since both sets of cores come from similar zones. A preferable ex planation might be that some of Kennett's cores (1970), especially Ell-3, E15-16, E20-14, E21-17, and E21-18 are older than the Brunhes to Matuyama age assigned to them, or contain significant hiatuses, leading from Brunhes into Gauss, just as in some cores of the present study (Fig. 14A, 16). Paleomagnetic analysis of the cores (Goodell and Watkins, 1968) is not contradictory to such an as sumption. It would even support this interpretation in E15-16 and E21-17. E21-18 has a complicated alternation of reversed and normal portions in its upper half that 135 might represent lower Matuyama to Gauss. If the cores in question are primarily Gauss, the ranges of the above species (Kennett, 1970) are reconciled with the present findings, and Kennett's zonatlon (Table 2), mainly based on regional events, can be compared with the zones pro posed earlier. Interestingly, the ranges of G. nunctl- oulata and £.. lnflata roughly overlap 1.5-1.6 m.y. In the present area (Fig. 13); In Kennett's material the equiva lent overlap rarely takes more than one meter of sediment (foramlnlferal ooze), which amounts to significantly less time at normal deep-sea sedimentation rates. This would Indicate that g,. nunctloulata left the Pacific sector of the southern oceans before It emigrated from the present localities. The lack of overlap and the discontinuous range of G. truncatullnoldes In some of Kennett's cores could also be the result of hiatuses and reworking. As shown later, even Th^® analyses can be misleading, since downward displacement of Holocene material can be veri fied in many Instances. There is a general accordance between the present foramlnlferal ranges and those occurring In the North Pacific S3CP drillings (Olsson and Goll, 1970; Olsson, 1971; and Fig. 13 of present study). The minor dif ferences are explained by the authors' Indirect correla tion with the paleomagnetic scale and by climatic dif ferences. It Beems that G. lnflata s.s.. appeared In the 136 North Pacific area approximately 1.0 m.y. (upper Gauss) after Its first record In subantarctlc-antarctlc areas. It must be remembered, though, that water masses over the DSDP sites are considerably warmer than over the local ities of the present cores. It had already been alluded to the remarkable agree ment between the ranges of some Indices In E39-76 and those given for the same species by Hays and others (1969) and Ujlle and Mlura (1971)• Figure 13 illustrates the ap propriate data. Except for the presence of the G. mlozea lineage in the present cores and the New Zealand upper Miocene- Pllocene sections, correlations between both areas are difficult to establish. Nevertheless, the presence of atypical G. mlozea mlozea (PI. 2, figs. 4, 5), G. mlozea oonoldea and G. mlozea snherlco-mlozea in the oldest Gil bert foraminlferal samples (E39-67, 56, and 48; Gilbert "b" and slightly older; Figs. 13, 14B, E, F) correlate this part of the cores with latest Tongapurutuan-earliest Kapitean (Walters, 1965; Jenkins, 1971; Fig. 15 of present study). Consequently, paleomagnetic ages for this part of the New Zealand Neogene should be Gilbert "b" and older. The concurrence of G. mlozea conoldea and G. mlozea snherl- comlozea In the remaining Gilbert and the lower two thirds of the Gauss should correlate with an equivalent concur rence of these forms in the New Zealand Kapitean and low 137 est Opoitlan (Pliocene) ae shown In Figure 15* Paleo- magnetic analysis of New Zealand Pliocene-early Pleisto cene sections (Kennett and others, 1971) agree remarkably well with these conclusions for the Opoitlan Stage. It was found to be mostly Gauss. One striking facet of the zonatlons proposed here and by other authors Is the coincidence of some zonal boundaries (Fig. 15)• For example, the base of the S. peregrlna-L. heteronoros Zone correlates with Gilbert "b", Just below the base of the G. mlozea oonoldea Zone. The C. blcornls Zone commences in the upper Gauss at al most the same level the G. truncatullnoldes Zone begins and at the point where the North Pacific L. heteronoros Zone has its lower boundary (Hays, 1970). The first ap pearance of S. neregrlna (about 5*0 m.y.b.p., Fig. 13) de fines the base of the presently proposed S. neregrlna Zone and that of the tropical S. neregrlna Zone (Fig. 14). Its extinction, on the other hand, defines the base of the present C. blcornls Zone and that of the tropical Pterooanlum nrlsmatlum Zone. In addition, the top of the present C. blcornls Zone is Isochronous to the top of the tropical P. nrlsmatlum Zone and, in turn, coincides with the Pllocene-Plelstocene boundary (Fig. 15)• In summary, the boundaries of four tropical radiolarian zones (Rledel and Sanfillppo, 1971) are comprised between latest Epoch 5 and latest Gauss, namely the top of the QmmfttartuB penultlmus Zone and the bases of the S. neregrlna Zone, the Snongaster nentas Zone, and the P. nrlsmatlum Zone (Pig. 15). r i MIOCENE-PLIOOENE BOUNDARY AND THE MAGNETIC SCALE To simplify the discussion, it is best to circum vent momentarily the implications of the type-section con cepts and to refer strictly to deep-sea correlations. In terms of Blow's (1969) Neogene planktonic foramlniferal zonation, there are only minor disagreements among workers regarding the placement of the Mlocene-Pliocene boundary. Some prefer to place it within Zone N18 (Blow, 1969; Berggren, 1971a) and others would rather choose the top of this zone (Parker, 1967; Bandy and others, 1971; Bronnlmann and Reslg, 1971)* an approach favored here. Major differences are voiced, however, concerning its placement relative to the magnetic scale or other "absolute" scales. For example, Berggren (1971a) and Hays and others (1969) suggested ages of about 5.5 and over 4.5 m.y. respectively, both probably within the paleo- magnetic Epoch "5"» Bandy and others (1971), on the other hand, placed the boundary within the Gauss Epoch (top of Mammoth), at an age of approximately 3*0 m.y. Still dif ferent information is provided by a K-Ar date (Dymond, 1966) of 4.3! 0.3 m.y.b.p. obtained on an ash layer near the experimental Mohole Miocene-Pllocene boundary of 139 140 Martini and Bramlette(1963). In view of these dis parities, It Is increasingly difficult for the non- speclallst to form an opinion on this controversial boun dary. Reviewing the literature, it appears that foramini- feral workers, regardless of preference for a specific ’ 'absolute” date, most often define latest Miocene by the presence of Sphaeroldlnellopsls and absence of gphaerol- dlnella dehlsoens. and lowest Pliocene by the first ap pearance of S. dehlscens (in the form of S. dehlsoens im- matura). For all practical purposes, then, the evolution ary transition from Sphaeroldlnellopsls subdehlscens (without dorsal apertures) to S. dehlscens lmmatura (with a small dorsal sutural aperture), followed by the almost coincident extinction of the former, is probably the most widely applied criterlum to recognize the boundary. Con tinuing this argument, the presence of rare S. dehlscens lmmatura in E39-76 in the top of the Mammoth event and above (which Increase in abundance and in development of dorsal apertures higher in the core) would thus Indicate the vicinity of the Mlocene-Pliocene boundary slightly below the range of the core, perhaps still within the Mammoth. This reasoning is strengthened by findings of Glass and others (1967), Robinson and Lamb (1970), and 4 Ujiie and Mlura (1971), who also encountered the first S. dehlsoens in or just below the Mammoth event, and by the 141 development of Pullenlatlna obllqullooulata obllqullocu- lata slightly above the Mammoth, both here and In Hays and others (1969) material (Fig. 13)* The latter occurs first within N19, the earliest Pliocene zone. Bandy and others (1971) have come to almost Identical conclusions by re evaluating the work of previous authors. Thus, It appears that Hays' and others (1969) range of S. dehlscens. which extends Into basal Gilbert In V24-59 and V20-163, may have been the result of contamination. This seems especially likely considering the drastic reduction In numbers at the Mammoth. It needs to be emphasized that except for the S. dehlscens datum of Hays and others, all major extinctions and appearances, which occurred during the Gauss (Table 5) have generally similar ages In the few paleomagnetic studies available today (Glass and others, 1967; Hays and others, 1969; Robinson and Lamb, 1970; Bandy and others, 1971; Ujiie and Mlura, 1971; present paper). Consequently, employing tropical planktonlc foramlnlfera, one Is left with two choices In placing the boundary: (l) to accept Hays and others (1969) total range of S. dehlscens (based on two cores) and assign the boundary an age In excess of 4.5 m.y. (lower Gilbert or older), or (2) to use data presented by Glass and others (1967, four cores), Robinson and Lamb (1970; sections In Jamaica), Ujlle and Mlura (1971; core V21-98, Philippine Sea), the present study Table 5* Evolutionary events during Gauss Magnetic Epoch, low to high latitudes Snecies AnDroximate age Reference 1. Extinctions a. Foraminifera Snhaeroidinellonsis subdehiscens Above Mammoth 1. 2, 4, 5, 7 Globoauadrina altisnira s.l. Between events, upper Gauss 2, 4, 5, 7 Globorotalia miozea conoidea Upper Gauss 8 G. miozea snhericomiozea Upper Gauss 8 G. marearitae Base or top of Gauss 5, 7 b. Radiolaria Stichocorvs nereerina Above Kaena ro 00 PrunonvUe titan Above Kaena 5, 8 Lychnocanium arande Above Kaena 5, 8 Desmospyris snoneiosa Top of Gauss 6 Helotholus vema Top of Gauss 6 i - * 4 s - ro Table 5. Evolutionary events during Gauss Magnetic Epoch, low to high (continued) latitudes Snecles Annroximate aee Reference c. Diatomacea Thalassloslra convexa Top of Gauss 2 Cosclnodlscus aeelnis Lower Gauss 2 Actlnocvclus ellinticus var. lanceolata Base of Gauss 2 2. Appearances a. Foraminifera Snhaeroldlnella dehlscens Top of Mammoth 1, 2, 5. 7, 8 Globorotalia tosaensis Below Mammoth ro 00 G. truncatullnoldes (oresent area) Lower Gauss 8 Pulleniatlna obllauiloculata s.s. Between events 2, 5. 8 Globiaerinoldes saccullfer flstulosus Upper Gauss 1, 2, 5, 7 . & ■ V > i Table 5. Evolutionary events during Gauss Magnetic Epoch, low to high latitudes (continued) SnecleB Approximate age Reference b. Diatomacea Rhlzosolenla praebergon11 Middle Gauss 2 References: 1. Glass and others, 1967; 2. Hays and others, 1969; 3. Hays, 1970; 4. Robinson and Lamb, 1970; 5. Bandy and others, 1971; 6. Hay8, 1971; 7. UJlie and Mlura, 1971; 8. This study. 144 145 (£39-76), and the reinterpretations of previous work by Bandy and others (1971)> all of which show S. dehlscens to evolve in the Gauss (near the Mammoth event), with an ap proximate 3.0-m.y. age for the boundary. Obviously, the latter choice is preferred here. It is the only one compatible with £39-76, and it also is coincident to the extinction of Miocene radlolarians and foraminifers within the Gauss Epoch (Table 5). Thus, although the exact level of the boundary may be an arbitrary decision to some extent variable from core to core, the Gauss, and especially the upper Gauss, comprises a natural transition between faunas of different ages (Figs. 13, 15* Table 5). At this point is is convenient to refer briefly to the Messinian in the Pasquasia-Capodarso sections and the Trubi marls of Italy, generally accepted as uppermost Miocene-lowermost Pliocene stratotypes. Several authors (for example: Parker, 1967; Blow, 1969; Colalongo, 1970; Bandy and others, 1971; Lamb and Beard, 1972) have dis cussed faunal and stratlgraphlc implications of these sections, often voicing contradicting opinions. The fact remains, however, that the topmost Messinian can be cor related with Zone N18 (Blow, 1969; Colalongo, 1970; Bandy and others, 1971), and that the Trubi beds correlate with part of N18 and all of N19 (Parker, 1967; Blow, 1969; Bandy and others, 1971). In addition, S. dehlscens lm- matura evolves within these strata just below the N18/N19 146 boundary (Parker, 1967)• Consequently, assuming that the evolution was lsoohronous, this level In the Trubi beds should correlate roughly with the Mammoth event. Outside the tropical belt, a definition of the Mlocene-Pllocene boundary Is hampered by the lack of sphaeroldlnellas and other warm-water forms. In New Zea land (Jenkins, 1970, 1971). for example, the boundary Is placed between the Kapitean and Opoitlan Stages, and recognized by the first evolutionary appearance of G. punctlculata padana (= G. lnflata of New Zealand workers). This evolution Is thought to have commenoed during latest Kapltean-earllest Opoitlan (Mclnnes, 1965; Walters, 1965)* transgressing the boundary. In the present material, rare G. punctlculata padana (= G. lnflata of New Zealand) are found already In middle Gilbert, almost 1.6 m.y. before the ultimate extinction of G. mlozea spherloomlozea and G. mlozea oonoldea. which occurred simultaneously In the low est Opoitlan and the upper Gauss of the present cores. In contrast to New Zealand, In the present cores the evolu tionary change spans a much longer Interval. Since all o cores were collected from 5 to 10 S of the New Zealand Mlocene-Pllocene localities (under colder water-masses), this could result from climatic Influences. Furthermore, G. punctlculata padana. before only known from the Plio cene, has now been recorded in the top of the Messinian neostratotype (Colalongo, 1970) together with G. mlozea 147 spherlcomolzea (= G. mlozea saphoae Blzon of Colalongo)* and G. craesula oonomlozea. The latter is considered to he characteristic of upper Miocene (Kapitean) In New Zealand (Jenkins, 1970). As defined today* the New Zealand boundary falls therefore within the top of the Messinian (upper Miocene) of Italy on one side* and below Gilbert "b" In the present material. Since most of the Opoitlan Stage Is Gauss (Kennett and others, 1971; present paper), this is obviously below Its first occurrence in New Zea land, and is therefore time transgressive. A preferable alternative is the usage of the G. mlozea conoldea and G. mlozea spherlcomlozea extinction data. They correspond to upper Gauss (Table 3, Fig* 13) and thus are near the S. dehlscens datum of the tropics. In addition, they coincide with the extinction of other Miocene microfossils. Since the G. mlozea lineage has now been recognized in a number of cold to temperate localities In both hemispheres (see dlsoussion of species) and In one tropical Indian Ocean core (Bandy, pers. comm.) with comparable stratigraphlc ranges, usage of this lineage would allow better world wide correlations than the earlier “G. lnflata” datum of New Zealand authors. In contrast with foraminiferal specialists, radio- larian workers have devoted considerably less attention to the Mlocene-Pllocene boundary problem. Hiedel and San- fHippo (1970) drew a boundary in the lower part of the 148 tropical Spongaster pentaa Zone, which other studies have generally followed (Moore, 1971; Casey, 1972; Casey and others, 1972). Thereafter, Rledel and Sanflllppo (1971) preferred to leave this level unspecified. It has been shown earlier that the top of the S. pentas Zone (as de fined by the Stlchocorys neregrlna extinction datum) Is correlative with the upper Gauss. Therefore, Rledel and Sanflllppo's (1970) boundary is probably also located Within the middle or lower Gauss, perhaps not far from the S. dehlscens datum near the Mammoth event. Casey (1972) and Casey and others (1972) have arrived at virtually the same correlation for this boundary by comparing the paleo- magnetlc and radlolarian stratigraphy of core E14-8 with radlolarlan sequences In Mlocene-Pllocene sections of southern California. Regardless of the need to establish a boundary for purely practical purposes, the Gauss, and especially the upper Gauss, still represents a transitional period of profound faunal changes. Many microfossils with Miocene ranges become extinct, and new forms, restricted to Pliocene-Holocene appear, both in the tropics and high latitudes (Table 5; Fig. 13). These faunal changes have been documented by Hays and Opdyke (1967; top of Gauss) in antarctic cores, by Hays and others (1969; middle of Gauss) in tropical Pacific sediments, by Casey and Sloan (1971) within the Monterey Formation, southern California 149 (where the authors noticed a drop In diversity Just above the local Mlocene-Pllocene boundary correlated with the upper Gauss by Casey and others, 1972), and are obvious In the upper Gauss of the present cores. In conclusion, a Gauss Mlocene-Pllocene boundary, even one defined arbi trarily by easily recognized events, is therefore In ac cord with the transitional character of this magnetic epoch. r i SEDIMENTARY RECORD Sedimentation Rates Plots of magnetic polarity boundaries against time In core (Fig. 17) provide a reasonably accurate measure of sedimentation rates. In the present area the highest value that can be measured In this way corresponds to core 39-56, a siliceous clay which has a rate of about 2.0 cm/ 1000 yr. E39-58, and a short calcareous clay to ooze which has a slightly lower rate. E39-24 (not plotted since It did not contain any known events), a siliceous-calcareous clay, has a minimum rate In excess of 2.0 cm/1000 yr. E39-76 (calcareous clay) had an intermediate rate (about 1.5 cm/1000 yr), but due to difficulties of Interpretation It is not included in Figure 17. E39-48, 44, and 40, two calcareous oozes and one calcareous-siliceous clay, registered the lowest values (0.3-0.5 cm/1000 yr). In general, these sedimentation rates are In keeping with similar estimates made In adjacent areas by Vatklns and Kennett (1972) and Conolly and Payne (1972). Connolly and Payne (1972) estimated average sedi mentation rates of about 0.5 cm/1000 yr for the Srunhes Epoch in the general area of the Australian-Antarctic Rise. A tentative calculation of Gauss and Gilbert rates can be 150 r Figure 17. Plots of polarity events against time of selected cores. Note latest Gauss-latest Brunhes discon- formity In E39-44 Inferred from the blostratlgraphlc Interpretation In Figure 16. Approximate sedimenta tion rates range from 2.0 cm/1000 yr (E39-56) to 0.3 cm/1000 yr (E39-40). 151 MILLIONS OF YEARS B . P . GILBERT BRUNHES \ C M C M C O u> 3ST made by averaging sediment thickness for each epoch. These calculations are subject to several errors, but they convey an Idea of total sediment thickness. The average Gauss rate Is about 0.5 cm/1000 yr, identical to Conolly and Payne's Brunhes figure. A slightly higher value is estimated for the Gilbert (0.6 cm/1000 yr). If the central ridge area has an average age of about 10-20 m.y. (Weissel and Hayes, 1972), then these values support seismic pro filing observations by Houtz and Markl (1972) who found sediment covers adjacent to the ridge to be less than 100 m in thickness. Fauna! Reworking Reworking and hiatuses are thought to be common features of deep-sea cores. Most previous paleomagnetlc- blostratlgraphic studies, however, failed to show the ex tent to which such phenomena occur, mainly because the few cores studied were carefully selected to exclude Ir regularities. In contrast, the present material offers an opportunity to show precisely how complex the stratigraphy of "normal" deep-sea cores can be. Although based pri marily on the 12 paleomagnetlcally dated cores, the en suing discussion tacitly Includes all cores studied (Table 1). Figure 12 showed a generalized correlation of polarity logs with the magnetic scale in which only major disconformitles were considered. By evaluating the de tailed faunal Interpretations (Figs. 14A-H, 16) and esti mates of sedimentation rates (Fig. 17)» several additional hiatuses can be shown to exist. It Is extremely difficult to define sedimentary Incongruities Involving Brunhes and Gauss (paleomagnetlcal- ly they cannot be distinguished unless the Gauss events are present) due to the lack of Indices that define upper Brunhes In these latitudes. Negative evidence Is meaning less In such circumstances. Th^^-measurements were per formed on E39-40 and 56 to test for Brunhes contaminations (Ku and Theyer, In preparation) In the cores. £39-40 Is typical for most cores In that It contains about 60-70 cm of upper Brunhes (t = 0.3 m.y.) mixed with Gauss In Its top, followed by Gauss Bedlments below (Fig. 14G). A thin layer of foramlnlferal tests stained by ferromanganese coatings mark the boundary. Since growth rates of a few mm/1000 yr are characteristic for deep-sea manganese nodules (Ku and Broecker, 1969), this layer probably represents a surface of extremely slow sedimentation and consequent long exposure to the water. This Is also evident In E39-44 and 42 (Fig. 16). No Th^°-activity was detected in the top of E39-56, Indicating that It Is probably one of the few cores In the area that does not contain a late Brunhes In Its top (Fig. 14E). At this point, Kennett's (1970) zonatlon of southern Pacific cores should again be reviewed. Sped- 155 flcally, some of his cores were dated also by the excess Th2^°-method. The 0.3-m.y. lsochron Is located, re spectively, at about 180 and 280 cm In cores £21-17 and E15-16 (Geltzenauer, 1969). This Is precisely at the base, or just below, two major reversed events In both cores (Goodell and Watkins, 1968). Several possibilities for Interpretation arise. After seeing the complexities In the present cores, It Is not farfetched to explain the apparently Incompatible results by assuming that the Th^°-lsochron represents the age of Brunhes contamina tions (as In E39-40), and that the paleomagnetlc record Is essentially correct. Bating E39-44, for example, would probably give very similar results (Pig. 16). Gauss-Brunhes Dlsconformlty An estimate of the age of the regional dlsconformlty described by Watkins and Kennett (1971, 1972) can be made with the aid of Figure 12. In the area of the present cores, the age of the core tops (below the Brunhes layers) range from at least 2.4 to at the most 3.3 m.y., with an approximate mode of 2.6 m.y. This Is similar to the ages Conolly and Payne (1972) estimated for the same feature along the Tasman fracture zone. Moreover, It Is virtually Identical to the age Watkins and Kennett (1972) obtained (2.5 m.y.) for what they considered to be the center of the dlsconformlty by plotting maps of second order trend 156 surface on the ages of their material. In contrast with the previous authors, the present study shows that there Is no systematic decrease of ages In specific directions, except that cores considerably south and north of the ridge (not Included here) contain normal Brunhes sedimenta tion. Furthermore, preliminary analysis of tops of cores collected west of the present area by EltanIn cruise 45 demonstrates that these also contain Gilbert and Gauss faunal assemblages In the vicinity of the ridge. Con sequently, the dlsconformlty first described by Watkins and Kennett (1971), and thought by them to be centered south of Tasmania, Is significantly greater In extension and generally consistent In Its Gauss age. It would not be surprising under these circumstances If reevaluation of previous Eltanln material revealed a lack of Matuyama and Brunhes sediments In other areas of the southern oceans as well. One explanation for the discrepant ages assigned to parallel cores from Eltanln cruise 39 by Watkins and Kennett (1972) and the present writer is the differences In opinion regarding the appearance of G. truncatullnoldes. G. lnflata. and £.. punctlculata (Fig. 13). It is obvious that in a large-scale study of over 100 cores, such as undertaken by Watkins and Kennett, one can only determine the ages of a few samples in each core. Thus, several of the shorter cores, thought by these authors to be Brunhes 157 In age In view of their predominantly normal polarity, would probably be dated as Gauss after closer lnspeotion. Watkins and Kennett (1971* 1972) have plausibly suggested that erosion* In response to Increased bottom- water velocities from under 10 cm/sec to over 10 cm/sec* was the prime cause of the dlsconformlty. As most cores contain varying amounts of Brunhes sediments In their tops* some deposition occurred at least during the last 0.3 m.y.* raising the speculative possibility that velocities may be returning to lower values. Except for this suggestion and the larger extension of the feature favored here* nothing of significance can be added to their arguments; considering the characteristics of the dlsconformlty* their explanation Is highly probable. Their papers discuss In detail the necessary conditions and Implications of such a velocity change. r t PALEOCLIMATIC TRENDS The lack of continuous Brunhes-Matuyama sequences In the cores under study prevents clarification of the present controversy about climatic cycles during these epochs (Bandy and others, 1971; Kennett, 1972). In ad dition, the multiple hiatuses and mixed portions In the carbonate-rich cores, together with severe solution of foramlniferal assemblages in others, restricts usefulness of the material even for the well represented Gauss- Gllbert period. One Gauss-age core, rich in oarbonate and seeming ly undisturbed, is E39-63* Coiling ratios of Globorotalla pachyderms fluctuate indicating at least three coolings (Pig. 18) of which one occupies most of the Mammoth event. The Gilbert-Gauss boundary is marked by a warm interval that had also been discovered in E14-8 (Pig. 18, and Bandy and others, 1971). The failure to discern these Gauss cycles by earlier studies (Bandy and others, 1971; Kennett, 1972) is explained by the expanded representa tion of Gauss in core E39-63* The most pronounced faunal change of climatic origin in the cores was noted in E39-56 (Pig. 18), just above Gilbert "c". The core section prior to this level is the only one in which 158 Figure 18. Gilbert-Gauss paleoclimatlc trends and composite generalized paleoclimatic curve for the last 5.2 m.y. 159 < 0 ( I ) EI4-8 PALEOCLMATES E39-63 INFLUX OF DEXTRAL 6. PACHYOERMA E 39-56 GENERALIZED INFLUX OF WARM RADIOLARIA GENERALIZED RALEOCLIMATES EVENTS 0 6 9 - ^ H GILSA COLD WARM H ID BANDY A ND OTHERS, 1 9 7 1 0\ O 161 typical antarctic species of radlolarla (such as Spongo- trochus glaclalls. Llthellus nautlloldes. Spongpplegma antarctica) do not completely dominate the assemblages. Warm and temperate species (Fig. 14E) are common here. Above the level, a uniform cooling trend continues to about where Gilbert "b" should be located. At this point a minor warm Interval can be distinguished by a reduction of polar species. A second, gradual warming is encounter ed at the level of Gilbert "a". This information can be interpreted (Fig. 18) as Indicating that at least five major coolings must have occurred between about 5*0 and 2.6 m.y.b.p. Of these, the first two were short (<0.1 m.y.), whereas the other three lasted considerably longer (>0.1 m.y.) and were about equal In duration. Because of the lack of reliable Holocene surface material as a reference, It Is difficult to quantify these implied temperature changes. Extrapolation from live planktonic data on colling ratios of G. pachyderma (Be', 1969) would Indicate summer surface temperatures below 5°0 for the cold intervals of the Gauss at about 47°S (E39-63, Table l) and above 10°0 for the warmest peaks above the Mammoth and Eaena (Fig. 18). Keeping the limitations of such extrapolations in mind, this implies a northward shift of modern summer surface Isotherms by roughly ten or more degrees of latitude. Thus, the cold Intervals probably represent glaclatlonB comparable in magnitudes to those of the Pleistocene. Conversely, most warm Intervals would equal modern ambient temperatures at the same latitudes (compare surface temperature data of Kustanowlch, 1963). It follows that the warmest interval in the lower Gilbert and Epoch 5 (Fig. 18) must represent ambient temperatures in excess of those present today at the same latitudes. This is shown in the generalized paleoclimatic curve of Figure 18, and it agrees in broad terms with conclusions of Bandy and others (1971) based on cores ElA-8 and 13-17. The latter were collected in the southern Pacific in still higher latitudes than E39-56. Kennett (1968) has shown that in New Zealand the Tonga* purutuan and Kapltean upper Miocene Stages were marked by an increasingly colder climate and that the lower Pliocene Opoitlan was generally warmer. From earlier discussions (Fig. 15) it is known that these units correspond to most of the Gilbert and Gauss. Thus, with the exception of the greater detail shown here, the New Zealand sections (Kennett, 1968) corroborate a generally colder (perhaps glacial) environment for the Gilbert (Tongapurutuan- Kapitean) than during the Gauss (mostly Opoitlan), in which at least three short temperate cycles occurred (Fig. 18). Finally, the northward shift of warm*water planktonic foramlnlfers, found by Kennett (1968) to begin during the Tongapurutuan of New Zealand, probably correlates with the severe cooling above Gilbert "c". CONCLUSIONS 1. Magnetic stability and intensity of magnetiza tion cannot be predicted from knowledge of gross sedi ment lithology, although foraminiferal oozes generally show greater dispersion of NBM inclinations than other sediment types. Even after demagnetization, the inclina tions of most samples are lower than the angle of in clination of the ambient field at the core sites. A definite decrease in magnetic intensity is associated with the onset of reversals. 2. Adequate mlcrofossll control is crucial to the correct interpretation of the magnetic stratigraphies of cores. This is especially the case in an area like the present one, where Brunhes age sediments unconformably overlie Gauss age strata in many core tops. The polarity logs are further complicated by a number of short-period polarity events or deviations that do not correlate with the established magnetic scale. 3. The following five evolutionary radiolarian zones are proposed for the period comprised by latest Epoch 5 and latest Brunhes: 163 164 Stlchocorys delmontense Zone (?-5*0 m.y.p.b.) Stlchocorys perggglna Partlal-range Zone (5*0-4.2 m.y.p.b.) S. peregrlna-Lamorocyclas heteronoros Concurrent- range Zone (4.2-2.6 m.y.b.p.) Olathrocyclas blcornls Partlal-range Zone (2.6-1.8 m.y.b.p.) Stvlatractus unlversus Partlal-range Zone (1.8-0.4 m.y.b.p.) The boundaries of these zones are defined by evolutionary first appearances and extinctions. Some of these can also be recognized In the tropics and the North Pacific, therefore serving as a basis for world-wide correlations. 4. The following four evolutionary, planktonic foraminiferal zones are proposed for the period between middle Gilbert and latest Brunhes: Globorotalla mlozea mlozea Zone (?-4.2 m.y.b.p.) Globorotalla mlozea conoldea Partlal-range Zone (4.2—3•3 m.y.b.p.) G. mlozea conoldea-G. truncatullnoIdes Concurrent- range Zone (3*3-2.6 m.y.b.p.) 165 G. truncatullnoldes Partlal-range Zone (2.6-0 m.y.p.b.) The boundaries of the zones, just as those of the radlolarlan zonatlon, are based on evolutionary datum planes. Of these, the G. mlozea mlozea extinction datum and the G. mlozea oonoldea extinction datum permit cor relations with sections in New Zealand, the North Pacific, the North Atlantic, and, to some extent, even with cooler cycles of the tropical areas. 5. Globorotalla truncatullnoldes can be shown to have first appeared in the basal Gauss of the present area. This predates its initial appearance in lower latitudes by about 1.5 m.y. Globorotalla lnflata s.s. first appeared at about the level of Gilbert "b". Globorotalla ounctlculata s .1., present in the cores throughout the Gilbert and most of the Gauss, emigrated from the present latitudes at about 2.5 m.y.b.p. 6. In the northernmost core (E39-76, £&. 36° S) it was possible to indirectly recognize Neogene Zone 19 and to correlate it with middle to late Gauss on the basis of the concurrence of Snhaeroldlnella dehlscens immature and Pullenlatlna prlmalls. the first appearance of P. obllaulloculata. and the gradual development of S. dehlscens dehlscens. Paunal evidence similarly permitted correlation of upper Miocene to lower Pliocene stages of New Zealand with the paleomagnetic scale. Thus, uppermost 166 Tongapurutuan-lowest Kapitean correlates with paleo- magnetlc ages up to early Gilbert, the Kapitean Stage (uppermost Miocene) with mostly Gilbert-earliest Gauss, and the Opoitlan Stage (lower Pliocene) with mostly Gauss. 7. The Miocene-Pllocene boundary is, In practice, a more or less arbitrary level that varies according to faunal group and latitude. In antarctic-subantarctlc areas it is probably best placed in the late Gauss, at about 2.5-2.6 m.y.p.b., a level at which the fora- miniferal G. mlozea-llneage became extinct. This co incides with the extinction of the radiolarians Lvchno- caplum grande, Stlchocorys neregrlna. and Prunopyle titan. Regardless of the ultimate placement of the boundary, the fact remains that the Gauss Epoch was a period of biotic transition that can be recognized in all latitudes. Species of Miocene affinities became extinct and Pliocene-Holocene lineages appeared within it. 8. Average sedimentation rates in the area during the Gilbert (0.6 cm/1000 yr) were, apparently, slightly higher than during the Gauss (0.5 cm/1000 yr). The area under study is affected by an eroslonal disconformity which is responsible for the virtual lack of latest Gauss, Matuyama, and, in part, Brunhes age sediments. An average age of 2.6 m.y. distinguishes the base of this feature, but locally some Brunhes sediments have accumulated since at least 0.5 m.y.b.p. Thus, sediments equivalent to about 167 2.3 m.y. of latest Gauss, Matuyama, and Brunhes are generally missing in this area. The present study and un published data demonstrate that this erosional feature is significantly greater in extension than originally thought by other authors. An increase in bottom-current veloci ties (from less than 10 cm/sec to over 10 cm/sec), as suggested by previous studies, is the most plausible ex planation of its origin. 9. At least five cold cycles occurred during the Gllbert-Gauss period. Two were mild and lasted less than 0.1 m.y.; they are associated with latest Gauss and the Kaena event. The remaining three were severe and some what longer; they occurred, respectively, in the Mammoth event-early Gauss, the middle Gilbert above event "b", and the Middle Gilbert below event "b". A short, distinct warming spans the Gilbert-Gauss boundary. A long, con siderably warmer period, which represents temperatures in excess of those at the same latitudes today, began below the Epoch 5-Gilbert boundary and terminated just above Gilbert "c". 10. There was no discernible connection between faunal extinctions, climatic deteriorations, and magnetic reversals. It must be emphasized, however, that the pre sent cores are poorly suited for analyses of these rela tionships in view of the numerous anomalies found in the sedimentary and paleomagnetlc records. T TAXONOMIC NOTES Order: Foramlnlferlda Eichwald, 1830 Family: Globorotallldae Cushman, 1927 Genus: Globorotalla Cushman, 1927 Subgenus: Turborotalla Cushman and Bermudez, 1949 Globorotalla (Turborotalla) lnflata (d'Orblgny), 1839 Globorotalla (Turborotalla) InflLfcte trlaneula. n. subsp. (PI. 5, figs. 1-7) 1972 Globorotalla Inflata (variant) - Lamb and Beard, p. 53, pi. 27, figs. 1, 2, 5. Description of the holotvne: Test of moderate size, about 2 whorls in low, trochosplral arrangement, three chambers In last whorl. Dorsal side evolute, subquadrate in outline, flat to barely convex; center of dorsal side covered by translucent, smooth encrustation completely ob scuring earlier whorls. Ventral side Involute, sub quadrate to subtriangular in outline, strongly convex to subconlcal with broadly rounded apex. Chambers rapidly increase In size as added, dorsally renlform at first, subrectangular in the last whorl, 2 to 3 times longer than wide; ventrally, subtriangular, slightly inflated, embrac ing. Sutures dorsally invisible (in clarifying liquids, lntercameral sutures are straight to slightly curved and 168 169 almost tangential to spire); ventrally distinct, straight to moderately curved, flush to slightly depressed. Peri pheric view subtriangular, broadly rounded peripheric margin. Aperture a narrow, straight slit, entirely ventral, without lip. Walls smooth, polished, very finely perforate. Dimension of holotype: 0.4mm (diameter). Type locality: Holotype and 20 paratypes from core E39-76, collected at 36° 30'S, 161° 14'E, at 3785 m (Tasman Basin), and 945-950 cm within the core. Type level: Pliocene, middle of Gauss Magnetic Epoch, correlated with tropical Neogene zone N 19 (Pig. 14A). Remarks: The new subspecies is easily distinguished from Globorotalla lnflata lnflata by the highly vaulted to subtriangular ventral side, flat dorsal side, narrow slit- like aperture, and by the three non-globose, subtriangular chambers of the last whorl. There is some variation in the inflation of the chambers and specimens with 3i chambers in the last whorl do occur. Rare transitional specimens, between the new subspecies and the nominate subspecies, have also been found. These have 3& chambers, that are more inflated, and their apertures are low arches. Other characteristics are also transitional. As indicated in the synonymy, Lamb and Beard's 170 (1972) G. lnflata variants from the early Pleistocene of the Gulf Coast (which would approximately correlate with Gauss; J. H. Beard, pers. comm.) are within the range of the present subspecies. Specimens received from the authors are somewhat smaller and thinner than the present forms and also Include a greater number of transitional characters between the new subspecies and G. lnflata ln flata. If the age of Lamb and Beard's variants is truly Gauss, It would seem that the present subspecies Is re stricted to this epoch. Parker (1967) has Illustrated a G. lnflata variant from Indian Ocean core D0L0117 (164-166 cm) at a level correlated with Zone N21. Her specimens, although not unlike the new subspecies, are closer to transitional forms between the new subspecies and G. lnflata s,.s. There are no variations of G. lnflata comparable to the present subspecies In the Holocene (compare Yen, 1971). Its subspecific level Is supported by transitional speci mens to G. lnflata .s. s.., by the restricted distribution, and by the short stratlgraphlc range. r ACKNOWLEDGMENTS The writer expresses his most sincere gratitude to Dr. Orville L. Bandy under whose patient guidance this study was undertaken, and who also read the manuscript. Dr. B. E. Casey assisted during the initial phase of the radiolarlan work, discussed several aspects of the dis sertation, and kindly gave access to important, un published Information. Drs. J. H. Beard, K. Bostrom, N. de B. Hornibrook, J. C. Ingle, Jr., D. G. Jenkins, and R. K. Olsson contributed helpful data and suggestions or comparative material. Dr. T. L. Ku's participation with Th2^® analyses and stimulating suggestions is also sincerely appreciated. Drs. D. S. Gorsline and R. E. Pieper critically reviewed the manuscript indicating many possibilities for improvements. R. L. Fleisher and E. Vincent participated in stimulating discussions of the work, and T. C. Lee wrote the FORTRAN IV program used for the paleomagnetic computations. Special mention is made of the cooperation of Drs. A. Cox and C. H. Denham for, respectively, giving permis sion to use the Stanford University spinner-magnetometer and related facilities, and for crucial assistance during the paleomagnetic work at Stanford. 171 172 A better appraisal of the area under study was pos sible due to the generosity of Drs. D. E. Hayes, J. R. Conolly, J. P. Kennett, R. R. Payne, and N. D. Watkins who kindly provided unpublished geophysical data and preprints of forthcoming papers. Appreciation Is also extended to the officers, crew and other participants on cruise 39 of the U.S.U.S. EltanIn for making the collection of the cores possible. Sincere thanks go to the Office of Polar Programs of the National Science Foundation for support under grant GV 25749. Some aspects of the study were supported by the Oceanographic Section, National Science Foundation, grant GA-34145. PLATES The USC No. following the species names In the captions Is the collection number assigned to the hypotypes. The measurements given In mm refer to the greatest dimension of the hypo- types; those In cm Indicate sampling levels within the cores. 173 PLATE 1 SELECTED RADIOLARIAN INDICES (Figs. 1-12 from E39-56; figs. 13-17 from E39-48) Figure 1. Stlchocorys peregrine (Rledel), USC No. 1512; 0.28 mm; 1315-1317 om. 2. Stlohooorys peregrlaa (Rledel), USC No. 1513; 0.20 mm; 1315-1317 om. 3* Prunoovle titan Campbell and Clark, USC No. 1514; 0.17 mm; 1315-1317 cm. 4. Desmospyrls sponglosa Hays, USC No. 1515; 0.10 mm; 1315-1317 cm. 5. Clathrocyclas blcomls Hays, USC No. 1516; 0.25 mm; 1315-1317 cm. 6. Cannartlsous marylandlous Martin, USC No. 1517; 0.20 mm; 1315-1317 cm. 7* Proseepa bp. (digitate), USC No. 1518; 0.30 mm; 1315-1317 cm. 8. Theooyrtls redondoensls Campbell and Clark, USC No. 1518; 0.l6 mm; 1315-1317 cm. 9. Eucyrtldlum oalvertense Martin, USC No. 1519; 0.16 mm; 1315-1317 cm. 10. Qyrtocapsella tetraptera Haeckel, USC No. 1520; 0.14 mm; 1315-1317 cm. 11. CalocTOlas §£., USC No. 1521; 0.22 mm; 1315-1317 cm. 12. Calocyclas margatensls Campbell and Clark, USC No. 1522; 0.16 mm; 1315-1317 cm. 174 175 Figure 13. Iransltlonal specimen between 0. margatensls and Lamprocyolas heteronoros. USC No. 1523; 0.12 mm; 0.12 mm; 705-?l0 cm. 14. Iransltlonal specimen between C. margatensls and L. heteronoros. USC No. 1524; 0.15 mm; 705-710 cm. 15. Primitive specimen of L. heteroporos. USC No. 1525; 0.15 mm; 705-710 cm. 16. lamprocvclas heteronoros Hays, USC No. 1526; 0.16 mm; 705-710 cm. S ' J *.* V . f t O t JS / ' i ,k\ W ' T i A ■ - •?* W-A V : K : A > Q j ,j\ < ■ mV j » * ■ ss ^ - - \ ; i , ■ . - S ^ ' 1 't •'“ 5 ■ “ - A . A - . ^ » « . , * , M ^ ' 1 - ^ ‘ A ’ V A V/ '4a / r. : v; • V A ;-r" A ; . ‘A # V jj4" 9Z.I PLATE 2 SELECTED PLANKTONIC FOHAMINIFERAL INDICES (All figures represent different specimens) Figure 1-3* Globorotalla mlozea mlozea Finlay, USC Nos. 1527-1529; E39-67, 985-990 cm (Is ventral view, O.56 mm, 2s side view, 0.44 mm, 3: dorsal view, 0.40 mm). 4-5. Globorotalla mlozea mlozea Finlay (atyploal, phylogenetloally advanced forms), USC Nos. 1530- 1531; E39-48, 805-810 cm (4: ventral view, 0.22 mm, 5s side view, 0.30 mm). 6-9. Globorotalla mlozea conoldea Walters, USC Nos. 1532-1535, E39-40, 105-110 cm (6: ventral view, 0.46 mm, Is ventral view, 0.40 mm, 8: side view, O.36 mm, 9s dorsal view, 0.42 mm). 10-12. Globorotalla mlozea snherlcomlozea Walters, USC Nos. 1536-1538, E39-40, IO5-IIO cm (10s side view, 0.46 mm, 11s ventral view, 0.46 mm, 12s dorsal view, 0.50 mm). 13-15. Globorotalla nunctloulata nadana Dondl and Papettl, USC Nos. 1539-1541, E39-40, 105-110 cm (13: ventral view, 0.32 mm, 14s side view, 0.30 mm, 15s dorsal view, 0.40 mm). 16-18. Globorotalla nunctloulata nunctloulata (Deshayes), USC Nos. 1542-1544, E39-40, 105-110 cm (16s ventral view, 0.56 mm, 17s side view, 0.60 mm, 18s dorsal view, 0.50 mm). 19. Globorotalla lnflata lnflata (d'Orblgny), USC No. 1545, E39-40, 105-110 cm, 0.54 mm, ventral view. 177 178 Figure 20-24. Globorotalla oraseaformlB Galloway and Wlssler, USC Nob. 1546-1950, E39-76. 825-830 cm (20: side view of variant 1, 0.40 mm, 21: ventral view of variant A, 0.50 mm, 22: ventral view of variant A, 0.60 mm, 23: ventral view of variant B, 0.50 mm, 24: dorsal view of variant B, 0.50 mm). 179 PLATE 3 SELECTED PLANKTONIC FORAMINIPERAL INDICES (All figures represent different specimens) Figure 1-3* Globorotalla crassaformla Galloway and Wlssler, 4.1., USC Nos. 1551-1553 (1: side view of variant B, 0.40 mm, E39-76, 825-830 cm; 2: ventral view of variant C, 0.44 mm, 3: side view of variant C, 0.34 mm, both from E39-67, 205-210 cm). 4-5. Globorotalla o£. crassula viola Blow, USC Nos. 1554-1555; E39-67, 405-410 cm (4: ventral view, 0.42 mm, 5: dorsal view, 0.36 mm). 6-11. Globorotalla truncatullnoldes (d'Orbigny), USC Nos. 1556-1566 (d>: dorsal view, 0.50 mm, 7: ventral view, 0.42 mm, 8: side view, 0.40 mm, 9: ventral view, 0.46 mm, 10: side view, 0.36 mm, all from E39-63; 355-360 cm; 11: side view, 0.32 mm; E39-40, 105-110 cm). 12-14. Globorotalla tosaensls Takayanagi and Salto, USC Nos. 1567-1569; E39-76 (12: ventral view, 0.42 mm, 13: dorsal view, 0.36 mm, both from 895- 900 cm; 14: dorsal view, 0.40 mm, 265-270 cm). 15-16. Pullenlatlna primalIs Banner and Blow, USC Nos. 1670-1571; E39-76, 805-810 cm (15: apertural view, 0.30 mm, 16: spiral view, 0.36 mm). 17. Pullenlatlna obllaulloculata ptllqulloppJ.a^a (Parker and Jones), USC No. 1572; E39-76, 705- 710 cm, 0.46 mm, apertural view. 18. Pullenlatlna obliaullooulata finalis Banner and Blow, USC No. 1573; E39-76, 5-10 cm, 0.50 mm, apertural view. 180 181 Figure 19-22. Sphaeroldlnella dehiscent? lmmatura (Cushman), USC Nos. 1574-1577; E39-76, 805-810 cm (19s dorsal view of typical specimen with small aperture, 0.36 mm, 20: dorsal view of typical specimen with slightly enlarged aperture, 0.42 mm, 21: dorsal view of advanced specimen with equatorially enlarged aperture, 0.40 mm, 22: apertural view of advanced specimen, 0.50 mm). 23. Sphaeroldlnella dehlscens dehlsoens (Parker and Jones), USC No. 1578; E39-76, 805-810 cm, 0.52 mm. 182 PLATE 4 Figure IA. Transitional specimen between Globorotalla trunca- tullnoldea (d'Orbigny) and G. tosaensls Takayanagi and Salto, USC No. 1579; E39-76, 715-720 cm, 0.38 mm. IB. Enlargement of the above specimen, showing the transition from an Imperforate keel on the last and penultimate chambers to no keel on the ante penultimate chamber. 183 184 PLATE 5 Figure 1. Globorotalla lnflata trlangula. n. subsp., holo- type, USO No. 1580; E39-76, 945-950 cm, 0.40 mm (1A: ventral view, IB: side view, 1C: dorsal view). 2-7. Globorotalla lnflata trlangula. n. subsp., para- types, USC Nos. 1581-1586; E39-76, 945-950 cm, different specimens (2: ventral view, 0.36 mm, 3: side view, 0.34 mm, 4: dorsal view, 0.38 mm, 5: ventral view, 0.42 mm, 6: side view, 0.36 mm, 7: dorsal view, 0.28 mm). 185 186 REFERENCES CITED 187 r i REFERENCES CITED Aokl, N., 1963. Pliocene and Pleistocene foraminifera from along the Yoro River, Boso Peninsula: Sci. Rents. Tokyo Kyoiku Daigaku, sect. C, v. 8, p. 203-227. Bandy, 0. L., 1963, Miocene-Pliocene boundary in the Philippines as related to late Tertiary stratigraphy of deep-sea sediments: Science, v. 124, p. 1290- 1292. _______, 1967, Problems of Tertiary foraminiferal and radlolarian zonations, circum-Paciflc area: in Eleventh Pacific Science Congress, Tokyo, 1960T Symposium 25, Tertiary Correlations and Climatic Changes in the Pacific, pp. 95-102, Sasaki, Sendai, Japan. _______, 1971, Recognition of Upper Miocene Neogene Zone 18, Experimental Mohole, Guadalupe site: Nature, v. 233, p. 476-478. . 1972, Variations in Globlgerlna bulloldes d'drbigny as indices of water masses:Antarctic Journal U. S., v. 7 (in press). Bandy, 0. L., Casey, R. E., and Wright, R. C., 1971, Late Neogene planktonlc zonatlon, magnetic reversals, and radiometric dates, Antarctic to the tropics, in Antarctic Oceanology I: Antarctic Research Ser., Am. Geophys. Un., v. 15, p. 1-26. Bandy, 0. L., Casey, R. E., and Theyer, F., 1972, Plank tonlc events, upper Gilbert-Gauss Magnetic Epochs: abstract submitted to 1972 Annual Geol. Soc. America meeting. Bandy, 0. L. and Ingle, Jr., J. C., 1970, Neogene plank- tonic events and radiometric scale, California: Geol. Soc. Amer., Spec. Paper 124, p. 133-174. Bandy, 0. L. and Wade, M. E., 1967. Miocene-Pliocene- Plelstocene boundaries in deep-water environments: Progress in Oceanography, v. 4, p. 51-66. 188 189 Banner, F. T. and Blow, W. H., I960, Some primary types of species belonging to the superfamily Globigerlnacea: Cushman Found. Foram. Res., Contrlb., v. 11, p. 1-41. _______, 1965, Progress In the planktonlc foraminiferal blg^trat^graphy of the Neogene: Nature, v. 208, p. . 1967, The origin, evolution and taxonomy of the foraminiferal genus Pullenlatlna Cushman, 1927: Micropaleontology, v. 13, P* 133-162. Be*, A. W. H., 1969, Planktonlc foraminifera: Antarctic Map Folio Series, Folio 11, p. 9-12, American Geo graph. Soc., New York. Beard, J. H., 1969, Pleistocene paleotemperature record based on planktonlc foraminifera: Gulf Coast Assoc. Geol. Soc., Trans., v. 19, p. 535-553* Berggren, W. A., 1968, Micropaleontology and the Pliocene/ Pleistocene boundary in a deep-sea core from the south-central North Atlantic: Glorn. Geol., ser. 2, v. 35, P* 291-312. _______, 1971 (1971a), Tertiary boundaries and correla tions: i& Micropaleontology of the Oceans, Cambridge Univ. Press, p. 693-809* _______, 1971 (1971b), Cenozolc foraminiferal blo- stratlgraphy and paleoblography of the North Atlantic: abstracts with programs, Geol. Soc. America, v. 3, p. 504. Blair, D. G., 1965, The distribution of planktonlc fora minifera In deep-sea cores from the Southern Ocean: Unpubl. M.Sc. thesis, Florida State Univ., 141 p. Blow, tf. H., 1969, Late middle Eocene to Recent plank- tonic foraminiferal biostratigraphy: Proc. 1st Intemat. Conference on Planktonlc Microfossils, Geneva, v. 1, p. 199-421. Bolli, H. M., 1966, Zonation of Cretaceous to Pliocene marine sediments based on planktonlc foraminifera: Venez. Geol. Min. Petrol., Bol. Inf., v. 9, P* 3-32. _______, 1970, The foraminifera of sites 23-31, Leg 4: i& Bader, R. G. and others, Init. Reports Beep Sea Drill ing ProJ., v. 4, p. 577-643, U. S. Govern. Printing Off., Washington, D. C. 190 Boltovskoy, E., 1966, Zonacion en las latitudes altas del Paclfico Sur segun los Foraminfferos planctonicos vivos: Rev. Inst. Nac. Invest, clenc. nat., Hidro- biol., v. 2, no. 1, p. 1-56. _______, 1969* Living planktonlc foraminifera at the 90° E meridian from the equator to the antarctic: Micro- paleont., v. 15# p. 237-255. Bronnlmann# P. and Reslg# J., 1971# A Neogene globigeri- nacean blochronologlc tlme-scale of the southwestern Pacific: .In Winterer, E. L. and others# Inlt. Re ports Deep Sea Drilling Proj., v. 7# p. 1235-1469. U. S. Govern. Printing Off., Washington, D. C. Campbell# A. S. and Clark, B. L., 1944, Miocene radio- larlan faunas from southern California: Geol. Soc. America, Spec. Publ. 51# p. 1-76. Casey, R. E., 1972# Neogene radlolarlan biostratigraphy and paleotemperatures: southern California, the experimental Mohole, antarctic core E14-8: Paleo- geography# Paleocllmatol.# Paleoecol., In press. Casey, R. E., Price, A. B. and Swift, C. A., 1972, Radlo larlan definition and paleoecology of the late Miocene to early Miocene In southern California: Amer. Assoc. Petrol. Geol., In press. Casey, R. E. and Sloan, J. R., 1971, Possible causes of diversities and extinctions of radiolarlans and other microplankton: Geol. Soc. America, abstracts with programs, v. 3, p. 763-765. Catalano, R. and Sprovleri, R., 1971, Blostratlgrafla dl alcune serie Saheliane (Messlnlano Inferlore) In Slcllla: Proc. 2nd Planktonlc Conference, Roma 1970, p. 211. Colalongo, M. L., 1970, Apuntl blostratlgrafici sul Messlnlano: Glorn. Geol., 36 (1968), 2, p. 515* Connolly, J. R. and Payne, R. R., 1972, Sedimentary pat tern within a continent-mid-oceanic ridge-contlnent profile: Indian Ocean south of Australia: In Ant arctic Oceanology II: The Australian-New Zealand sector: Antarctic Research Ser., Amer. Geophys. Un., v. 19, In press. 191 Cox, A., 1969, Geomagnetic reversals: Science, v. 163, p. 237-245. Dondi, L. and Pappettl, 1., 1968, Blostratlgraphlcal zones of Po Valley Pliocene: Glorn. Geol., v. 35, 3, p. 63. Dymond, P., 1966, Potassium-argon geochronology of deep-sea sediments: Science, v. 152, p. 1239-1251. Elttrelm, S., Gordon, A. L., Ewing, M., Ihorndike, E. M. and Bruchhausen, P., 1972 (1972a), The nepheloid layer and observed currents In the Indian-Pacific antarctic sea: Aa Studies In physical oceanography— a tribute to Georg Wust on his 80th birthday, Gordon and Breach, New York, In press. Elttrelm, S., Bruchhausen, P., and Ewing, M., 1972 (1972b), Vertical distribution of turbidity In the South Indian and South Australian basins: In Antarctic Oceanology: The Australian-New Zealand sector, Antarctica: Antarctic Research Ser., Amer. Geophys. Un., v. 19, In press. Friend, J. K. and Rledel, W. R., 1967, Cenozolc oro- sphaerld radlolarlans from troploal Pacific sedi ments: Micropaleontology, v. 13, p. 217-232. Geltzenauer, K. R., 1969, Coccollths as late Quaternary paleocllmatuw Indicators In the Southern Ocean: Nature, v. 223, p. 170-172. Glass, B., Erlcson, D. B., Heezen, B. C., Opdyke, N. D. and Glass, J. A., 1967, Geomagnetic reversals and Pleistocene chronology: Nature, v. 216, p. 437-442. Goodell, H. G. and Watkins, N. D., 1968, The paleo- magnetic stratigraphy of the Southern Ocean: 20° West to 160° East longitude: Deep-Sea Res., v. 15, p. 89-112. Gordon, A. L., 1971, Spreading of Antarctic bottom waters II: As, Studies In physical oceanography— a tribute to Georg Wust on his 80th birthday: Gordon and Breach, New York, In press. _______, 1972, On the Interaction of the antarctic clrcum- polar current and the Macquarie ridge: In Antarctic Oceanology II: The Australian-New Zealand sector: Antarctic Researoh Ser., Am. Geophys. Un., v. 19, In press. 192 Gordon, A. L. and Goldberg, R. D., 1970, Clrcumpolar characteristics of Antarctic waters: Antarctic Map Folio Ser., Am. Geogr. Soc., folio 13, p. 1-6. Griffiths, S. H., King, R., Rees, A. I., and Wright, A. £., I960, The remanent magnetism of some recent varved sediments: Proc. Roy. Soc. London, A, v. 256, p. 359- 383. Harrison, C. G. A., 1966, The paleomagnetism of deep-sea sediments: J. Geophys. R., v. 71, p. 3033-3043. Hayes, B. £. (ed.), 1972, Antarctic Oceanology II: The Australlan-Mew Zealand sector: Antarctic Research Ser., Am. Geophys. Un., v. 19* In press. Hayes, B. £. and Conolly, J. R., 1972, Morphology of the southeast Indian Ocean: is. Antarctic Oceanology II: The Australian-New Zealana sector: Antarctic Re search Ser., Am. Geophys. Un., v. 19, in press. Hays, J. D., 1965, Radiolaria and late Tertiary and Quaternary history of Antarctic seas: is Biology of the Antarctic seas II: Antarctic Research Ser., Am. Geophys. Un., v. 5» P* 125-184. _______, 1970, Stratigraphy and evolutionary trends of Radiolaria In North Pacific deep-sea sediments: Geol. Soc. America, Mem. 126, p. 185-218. _______, 1971, Faunal extinctions and reversals of the earth's magnetic field: Geol. Soc. America Bull., v. 82, p. 2433-2447. Hays, J. D. and Ninkovich, D., 1970, North Pacific deep- sea ash chronology and age of present Aleutian under- thrusting: Geol. Soc. America, Mem. 126, p. 263-290. Hays, J. B. and Opdyke, N. D., 1967, Antarctic Radiolaria, magnetic reversals and climatic change: SOience, v. 158, p. 1001-1011. Hays, J. B., Salto, T., Opdyke, N. D., and Burckle, L. H., 1969, Pllocene-Pleistocene sediments of the Equatorial Pacific: their paleomagnetic, biostratlgraphic, and climatic record: Geol. Soc. America Bull., v. 80, p. 1481-1514. Herb, R., 1968, Recent planktonlc foraminifera from sedi ments of the Brake Passage, Southern Ocean: Eclogae geol. Helv., 61, p. 467. 193 Houtz, R., Ewing, J., and Embley, R., 1971, Profiler data from the Macquarie ridge area: i& Antarctic Ocean ology I: Antarctic Research Ser., Am. Geophys. Un., v. 15, P. 239-245. Houtz, R. E. and Markl, R. G., 1972, Seismic profiler studies between Antarctica and Australia: In Antarctic Oceanology II: The Australian-New Zealand sector: Antarctic Research Ser., Am. Geophys. Un., v. 19, in press. Ingle, J. 0., Jr., 1967, Foraminiferal biofacies varia tion and the Mlocene-Fllocene boundary in southern California: Bull. Amer. Paleont., v. 52, p. 217- 394. Jacobs, S. S., Bruchhausen, P., and Bauer, E. B., 1970, Hydrographic stations, bottom photographs, and cur rent measurements, USNS Eltanln cruises 32-36. Lamont-Doherty Geol. Observ. of Columbia University, Palisades. N. Y., 460 p. JendrzeJewskl, J. P. and Zarlllo, G. A., 1970, Late Pleistocene paleotemperatures: slllcoflagellate and foraminiferal frequency changes in a deep-sea core: Antarct. Joum. U.S., v. 6, p. 178. Jenkins, G. D., 1970, Foramlnlferlda and New Zealand Tertiary biostratigraphy: Rev. Esp. Micropaleont., v. 2, p. 13. _______ , 1971, New Zealand Cenozoic planktonlc Foramini fera: New Zealand Geol. Survey, Paleontol. Bull. 49, p. 1-278. Kahn, M. I., 1972, Sedimentary structure, carbonate content, and displaced fauna in a Quaternary turbidlte sequence from the Great Australian Bight abyssal plain: Unpubl. term paper, Univ. of Southern Calif., 33 p. Keen, M. J., 1963, The magnetization of sediment cores from the eastern basin of the North Atlantic Ocean: Deep-Sea Res., v. 10, p. 607-622. Kennett, J. P., 1966, The Globorotalla crassaformls bio series in north Westland and Malborough, New Zealand: Micropaleontology, v. 12, p. 235. r i 194 Kennett, J. P., 1968, Paleo-oceanographic aspects of the foraminiferal zonatlon In the Upper Miocene-Lower Pliocene of New Zealand: Glorn. Geol., v. 35» 3* p. 143-156. _______, 1969 (1969a), Distribution of planktonlc Fora- minlfera in surface sediments southeast of Mew Zea land: Proc. 1st Intemat. Confer, on Planktonlc Mlcrofossils, Geneva, v. 2, p. 307-322. _______, 1969 (1969b), Foraminiferal studies of southern ocean deep-sea cores: Antarct. Journal, U.S., v. 4, p. 178-179. _______, 1970, Pleistocene paleoclimates and foraminiferal biostratigraphy in subantarctlc deep-sea cores: Deep- Sea Res., v. 17, p. 125-140. _______, 1972, South Pacific planktonlc foraminiferal bio geography and late Cenozoic paleo-oceanography: Amer. Assoc. Petrol. Geol., v. 56, p. 631. Kennett, J. P. and Geitzenauer, K. R., 1969, Pllocene- Pleistocene boundary in a South Pacific deep-sea core: Nature, v. 224, p. 899-901. Kennett, J. P. and Huddlestun, P., 1971, Subantarctlc Late Pleistocene climatic and paleoglacial fluctua tions: Antarct. Journal U.S., v. 6, p. 180. Kennett, J. P., Watkins, N. D., and Vella, P., 1971, Paleomagnetic Chronology of Pliocene-early Pleistocene climates and the Plio-Plelstocene boundary in New Zealand: Science, v. 171» p. 276-279. Ku, T. L. and Broecker, W. S., 1969, Radiochemical studies on manganese nodules of deep-sea origin: Deep-Sea Res., v. 16, p. 625-637. Kustanowich, S., 1963, Distribution of planktonlc Fora minifera in surface sediments of the south-west Pacific Ocean: New Zealand Journal Geol. Geophys., v. 6, p. 534-565. Lamb, J. L. and Beard, J. H., 1972, Late Neogene plank tonlc foramlnlfer8 in the Caribbean, Gulf of Mexico, and Italian stratotypes: Univ. Kansas Paleont. Oontrib., article 57 (Protozoa 8), p. 1-67. 195 Mclnnes, B. A., 1965. Globorotalla mlozea Finlay as ancestor to Globorotalla lnflata td'Orblgny): New Zealand Journal Geol. Geophys., v. 8, p. 104rl08. Margolis, S. V. and Kennett, J. P., 1971, Cenozolc paleo- glaclal history of Antarctica recorded In sub antarctlc deep-sea cores: Amer. Jour. Science, v. 271, p. 1-36. Martini, E. and Bramlette, M. N., 1963, Calcareous nanno- plankton from the experimental Mohole drilling: Jour. Paleontology, v. 37, p. 845-856. Moore, T., 1971* Radiolaria: 4n Tracey, J. and others, Inlt. Reports Beep Sea Drilling Project, v. 8, p. 727-775, U. S. Govern. Printing Off., Washington, D. C. Nakagawa, H., Niltsuma, N., and Hayasaka, I., 1969, Late Cenozolc geomagnetic chronology of the Boso Penin sula: J. Geol. Soc. Japan, v. 75, P* 267-280. Nakagawa, H., Niltsuma, N., and Elmo, C., 1971, Pliocene and Pleistocene magnetic stratigraphy In Le Castella area, southern Italy— a preliminary report: Quatem. Res., v. 1, p. 360-368. Ninkovlch, D., Opdyke, N. D., Heezen, B. C. and Foster, J., 1966, Paleomagnetic stratigraphy, rates of de position, and teprachronology in North Pacific deep- sea sediments: Earth and Planetary Sci. Letters, v. 1, p. 476-492. Olsson, R. K., 1971, Pliocene-Pleistocene planktonlc foraminiferal biostratigraphy of the Northeastern Pacific: Proc. Ilnd Intern. Conference on Planktonlc Microfossils, Rome, p. 921-928. Olsson, R. K. and Goll, M., 1970, Biostratigraphy: in McManus, D. A. and others, Init. Repts. Deep Sea Drilling Proj., v. 5, p. 557-567, U. S. Govern. Printing Office, Washington, D. 0. Opdyke, N. D. and Foster, J., 1970, Paleomagnetism of cores from the North Pacific: Geol. Soc. America Mem. 126, p. 83-119. Opdyke, N. D., Glass, B., Hays, J. D. and Foster, J., 1966, Paleomagnetic study of Antarctic deep-sea cores: Science, v. 154, p. 349-357. 196 Parker, P. L., 1967, Late Tertiary biostratigraphy (planktonlc foraminifera) of tropical Indo-Paclfic deep-sea cores: Bull. Amer. Paleont., v. 52, p. 115-208. Payne, R. R. and Conolly, J. R., 1972 (1972a), Turbidlte sedimentation off the Antarctic continent: In Antarctic Oceanology II: The Australian-New Zealand sector: Antarctic Research Ser., Amer. Geophys. Un., v. 19, in press. _______, 1972 (1972b), Pleistocene manganese pavement production: its relationship to the origin of manganese in the Tasman Sea: in Symp. on Manganese Deposits, NSP/IDOE, Columbia Univ., Harriman, New York, Jan. 20-22, 1972. Payne, R. R., Conolly, J. R. and Abbott, W. H., 1972, Turbidlte muds within diatom ooze off Antarctica: Pleistocene sediment variation defined by closely spaced piston cores: Geol. Soc. America Bull., v. 83, p. 481-486. Pitman, W. C. and Helrtzler, J. R., 1966, Magnetic anomalies over the Pacific Antarctic ridge: Science, v. 154, p. 1164. Rees, A. E., 1961, The effect of water currents on the magnetic remanence and anisotropy of susceptibility of some sediments: Geophys. J., v. 5, p. 235-251. Rledel, W. R., 1933, Mesozoic and late Tertiary Radio laria of Rotti: Jour. Paleont., v. 27, p. 805-813. _______ , 1958, Radiolaria: B.A.N.Z.A.R.E. Reports, ser. B, v. 6, p. 217-255. Riedel, W. R. and Sanfilippo, A., 1970, Radiolaria, Leg 4, Deep-Sea Drilling Project: in Bader and others, Inlt. Reports Deep Sea Drilling Project, v. 4, p. 503-575, U. S. Govern. Printing Off., Washington, D. C. _______ , 1971, Cenozolc Radiolaria from the western tropical Pacific: is. Winterer, E. L. and others, Inlt. Reports Deep Sea Drilling Proj., v. 8, p. 1529-1672, U. S. Govern. Printing Off., Washington, D. C. 197 Robinson, E. and Lamb, J. L., 1970, Preliminary paleo magnetic data from the Plio-Pleistocene of Jamaica: Nature, v. 227, p. 1236-1237. SanfHippo, A. and Riedel, W. R., 1970, Post-Eocene "closed" theoperid radiolarians: Micropaleontology, v. 16, p. 446-462. Takayama, T., 1967, First report on nannoplankton of the Upper Tertiary and Quaternary of the Southern Kwanto Region, Japan: J. Geol. B.A., v. 110, p. 169-198. Theyer, P., 1972, Globorotalla truncatullnoldes datum plane: evidence for an early Pliocene age in sub- antarctic deep-sea cores: Geol. Soc. America, ab stracts with programs, v. 4, p. 247. UJiie, H. and Mlura, M., 1971, Planktonlc foraminiferal analysis of a calcareous ooze core from the Philip pine Sea: Proc. 2nd Planktonlc Conference, Roma, 1970, p. 1231*1249. Vestine, E. H., Laporte, L., Lange, J., Cooper, C., and Hendrix, W. C., 1947, Description of the earth's main magnetic field and its secular change, 1903-1943: Carnegie Inst, of Washington, Publ. 578, p. 1-533. Walters, R., 1965, The Globorotalla zaelandlca and G. mlozea lineages: New Zealand Journal Geol. Geophys., v. 8, p. 109-127. Watkins, N. D., 1968, Short period geomagnetic polarity events in deep-sea sedimentary cores: Earth and Planetary Sci. Letters, v. 4, p. 341-349. _______, 1972, Review of the development of the geo magnetic polarity time scale and discussion of pro spects of its finer definition: Geol. Soc. America Bull., v. 83, p. 551-574. Watkins, N. D. and Kennett, J. P., 1971, Antarctic Bottom Water: major change in velocity during the late Cenozolc between Australia and Antarctica: Science, v. 173, p. 813-818. _______, 1972, Regional sedimentary disconformities and Upper Cenozolc changes in bottom water velocities between Australasia and Anarctlca: in Antarctic Oceanology II: The Australian-New Zealand sector: Antarctic Research Ser., Am. Geophys. Un., v. 19, in press. r t 198 Weissel, J. K. and Hayes, D. E., 1971, Asymmetric sea floor spreading south of Australia: Nature, v. 231, p. 518-521. Weissel, J. K. and Hayes, D. E., 1972, Magnetic anomalies In the southeast Indian Ocean: In Antarctic Ocean ology II: The Australian-New Zealand sector, Antarctica: Antarctic Research Ser., Amer. Geophys. Un., v. 19, In press. Yen, Z. M.-M., 1971, Environmental and geologic signifi cance of Globorotalla lnflata (d'Orbigny): Unpubl. M.Sc. thesis, Univ. of Southern California, Los Angeles, California, 104 pp. APPENDICES 199 APPENDIX I Numerical paleomagnetic data. Negative In clinations Indicate normal magnetization In the southern hemisphere. The samples were vertically oriented only; thus, declination data are not reliable and are Included solely for reference. Intensity of magnetization (M) Is expressed In emu, whereas the In tensity per volume (J) Is In emu/cm3 or gauss. 200 201 F 3 9 —22 4 8 51 S 12 6 01 t 40 78 M NI.'VI CM IN C L DECL M J 0 - 7 22 4 9 . 5 2 4 . 4 B 3 E - 0 A 1 1 2 1 F - C 4 10 - 3 9 80 4 0 . 9 7 4 , 1 1 O E -0 4 1 0 2 8 E - C 4 20 34 4 7 . 37 6 . 1 9 I E —0 4 1 S 4 8 E - 0 4 30 - 4 4 87 4 4 . 54 0 . 7 C 3 E -C 4 2 1 7 o F - C 4 40 - 2 4 41 8 8 . 1 7 1 . 5 1 f t E - 9 3 3 7 8 9 E - C 4 50 - 1 48 5 8 . 3 0 2 . 4 3 1 E - 0 J 6 C 7 8 E - C 4 fC - 3 7 27 5 2 . 3 7 8 . 6 2 0 E - C 4 2 1 5 5 E - 0 4 70 - 4 8 28 8 7 . 0 4 1 . 2 5 9 F - 0 3 3 1 4 8 K - 0 4 80 - 6 0 12 6 4 . 0 6 1 . 5 4 2 E - 0 3 3 8 5 4 5 —f 4 90 - 6 1 0 9 8 2 . 0 0 1 . 5 7 5 E - 0 3 3 9 3 7 E - C 4 1 00 - 3 7 64 6 3 . 3 6 1 . 2 9 9 E - C 3 3 2 4 8 E - 0 4 1 1C - 3 2 6 8 64 . C 2 9 . 6 6 6 E - 0 4 2 4 1 7E -C 4 120 - 7 3 94 6 5 . 1 5 1 . 0 6 7 E - 0 1 2 7 1 7 0 - 0 4 1 30 - 7 6 93 7 7 . 3 8 8 . 5 7 9 E - C 4 2 1 4 5 E - 0 4 140 - 6 9 55 6 8 . 1 2 6 . 4 6 5 F - 0 4 1 6 1 6 E - 0 4 1 50 - 7 9 37 71 . 4 9 7 . 2 2 B E - C 4 1 8 0 7 E - 0 4 1 60 - 7 4 93 7 4 . 9 8 3 . 7 6 5 E - 0 4 9 4 1 2 F - 0 5 1 70 - 8 7 16 4 4 . 9 5 3 . 7 0 4 E - C 4 9 2 5 9 E - 0 5 1 80 - 8 0 66 3 7 . 63 4 . 4 4 7 E - 0 4 1 1 1 2 T - C 4 19G - 6 7 31 5 8 . 9 7 6 . 6 5 6 E - 0 4 1 6 6 4 E - 0 4 20C - 6 9 83 6 . 33 6 . 6 1 OE-C 4 1 6 5 2 E - 0 4 2 1 0 - 7 2 59 2 6 . 5 4 9 . 4 1 4 E - 0 4 2 3 5 4 E - L 4 22C - 7 4 70 8 . 12 1 . 1 2 6 E - 0 1 2 8 1 6 E - C 4 2 3 9 - 7 7 79 3 . 8 1 1 . 4 9 6 E - 0 3 3 74 l f c - 0 4 2 4 0 - 7 4 04 6 . 5 7 1 . 9 9 9 E - 0 3 4 998F.-C4 2 5 0 - 7 1 41 5 5 . 4 3 1 . 2 7 8 E - 0 3 3 1 9 6 E - 0 4 26C — 63 29 8 7 . 18 1 . 1 9 2 E - 0 3 2 9 7 9 F - 0 4 2 7 C - 4 0 84 7 4 . 10 1 . 7 2 4 E -C 1 4 11 0 E -C 4 2 8 0 - 5 9 19 4 3 . 4 0 1 . 9 7 C E - C 3 2 6 7 5 F - C 4 2 9 0 - 7 5 85 21 . 7 8 9 . 2 6 5 E - C 4 2 3 1 6 E -C 4 3 0 0 - 6 4 82 4 3 . 0 7 5 . 5 3 9 E - 04 1 3 8 5 F - C 4 3 1 0 - 7 0 66 6 . 57 4 . 9 8 1 E - 0 4 1 2 4 5 E - C 4 3 2 0 - 6 6 44 4 . 3 9 6 . 8 3 7 F - 0 4 1 7 C 9 E -C 4 3 30 - 6 8 04 5 . 19 1 . 2 J 9 E - 0 3 3 0 9 7 E - C 4 3 4 0 - 6 7 6 8 1 2 . 0 8 7 . 9 0 3 E - 0 4 1 9 7 6 E - T 4 3 5 0 - 6 20 1 . 2 4 9 . 6 7 3 E - 0 4 2 4 1 8E -C 4 E 3 9 - 2 2 1ST DEMAG SAMPLS 1 C 0 - 8 0 0 Of CM IN C L DLCL M J C - 6 . 5 7 5 3 . 7 3 4 . 3 8 0 E - 0 4 1 . 0 9 5 E - C 4 50 - 3 . 8 5 6 0 . 9 5 1 . 5 5 b E - 0 3 3 . B 9 1 E - 0 4 60 1 3 . 0 0 5 6 . 2 5 1 . 3 9 2 E - C 4 3 . 4 6 0 E - C 5 170 - 8 2 . 7 5 5 1 . 2 8 3 . 2 2 3 F - 0 4 8 . 0 5 7 t : - C f 202 E 3 9 —22 2ND OEMAG SAMPLS 2 0 0 - 3 3 0 OF CM IN C L DECL M J 0 - 2 7 . 7 9 5 5 . 6 9 2 . 6 8 7 E - 0 4 6 . 7 1 8 F - C 6 50 - 1 . 1 6 6 3 . 3 6 I . 0 2 8 E - G 3 2 . 5 7 1 E - 0 4 E 3 9 - 2 2 3RD DEMAG SAMPLS SCO OE CM IN C L DECL M J 50 5 . 0 8 4 . 0 8 I . I 7 B E - 0 4 2 . 9 4 5 E - C 5 E 3 9 - 2 2 TRIGGF.P COME NRM CM IN C L DECL M J 60 - 6 2 . 4 3 7 0 . 9 5 1 . 5 3 2 F - 0 3 3 . B 2 9 E - 0 4 E39-24 51 35 S 126 09 F . 4352 M NPM CM IN C L DECL 0 - 2 6 51 77 90 IP “ 52 48 43 48 2G — 4 81 8 46 30 - 3 6 56 6 8 1 2 40 - 1 0 06 21 9 9 5C - 2 1 65 79 9 6 60 2 48 4 96 7C 2 48 2 49 BO - 3 4 9 8 6 7 14 90 1 26 14 C2 ICO - 1 5 26 72 9C 1 10 - 2 32 84 c a 120 - 3 14 69 00 1 30 - 3 2 24 79 1 3 1 40 1 50 86 P9 1 50 - 3 6 43 70 74 16C - 3 4 05 74 4 6 1 70 - 1 2 00 6 8 82 180 - 3 2 19 70 12 1 90 - 2 1 60 67 14 2 0 0 - 6 53 66 3C 2 1 0 - 4 4 00 4 2 62 2 2 0 - 1 7 83 66 90 2 3 0 - 1 4 57 51 2 8 24 0 - 3 51 5 9 17 2 5 0 - 1 0 90 6C 0 7 26 0 1 3 84 53 64 2 70 - 5 0 91 74 21 2 8 0 - 6 4 28 04 71 2 9 0 - 7 0 48 73 9 7 30 C - 4 0 27 73 2 2 3 1 0 - 3 ? 85 8 5 2 7 32 0 - 6 1 77 73 2 2 3 3 0 - 4 5 27 64 73 3 4 0 - 4 1 58 8 8 6 3 J5C - 30 1C 76 C 2 3 60 - 4 7 79 51 2 8 3 70 - 6 3 56 5 2 C 7 3 8 0 -1 22 12 2 5 39 0 - 2 9 84 47 28 40C - 4 1 54 4 3 70 4 1 0 - 3 6 95 57 39 42C - 1 9 15 6 5 4 8 4 3 0 - 3 4 06 60 0 5 4 4 0 - 2 9 1 3 72 33 4 50 - 4 0 74 6 5 96 4 6 0 - 4 4 23 71 4 9 47C - 3 1 1 1 51 0 8 4 8 0 - 3 9 98 44 9 5 4 9 0 - a 77 52 5 7 M J . 1 2 3 E - 0 3 1 8 7 1 F - C 4 • 4 7 9 E - 0 4 1 5 8 C E - 0 4 • 9 6 6 E —0 3 1 6 6 I E — P 3 • C 4 7 E -C 3 8 4 1 2 F - C 4 . 0 7 6 E -C 2 1 7 9 3 E - 0 3 • 9 0 5 E - U 3 6 5 C 8 E -C 4 .6 S 9 E - C 3 1 6 1 0 E - 0 3 • 6 3 2 F - 0 3 1 6 C 5 F - C 3 • 3 8 4 F - 0 3 2 36 7fc — C4 • 4 0 1 E - O J 1 5 8G C -C 3 • 3 3 1 E -C .3 5 5 5 l c - r 4 •C 9 1 E - C 3 5 1 5 1 E - 0 4 . 2 8 6 E - 0 3 3 8 1C E-C 4 • 1 7 1 E - 0 3 5 2 6 4 E - C 4 • 3 8 7 E - 0 3 3 9 7 8 F - 0 4 • 7 9 7 F - 0 3 6 3 2 9 F - C 4 . 6 9 2 E - C 3 6 1 5 3 F - 6 4 . 9 1 7 E - 0 3 6 5 2 8 E - 0 4 . 626F - 0 3 4 3 7 6 E - 0 4 . 4 3 9 5 - C 3 4 0 6 4 F - C 4 . 3 C 9 F - 0 3 5 51 1F -C 4 . 0 4 5 2 - 0 3 3 4 C 0 E -C 4 • 8 6 3 F - 0 3 4 7 7 2 E - C 4 • 9 7 8 E - 0 3 8 2 9 7 E - 0 4 • 0 70F - 0 3 5 1 1 7 F -C 4 • 9 7 6 E —0 3 6 6 2 6 E - 0 4 . 9 2 7 8 - 0 3 6 5 4 4 F - 6 4 . 3 C 9E -C 3 5 5 1 6 6 - C 4 • 2 0 0 E - C 3 5 3 3 J F - C 4 • 30 3 E - 0 3 3 83 8fc —C 4 • 0 0 3 F - 0 3 .3 33 8F — 6 4 • 8 4 8 F —0 3 3 0 HOE — C 4 . 774E —0 3 4 6 2 3F -C 4 • 3 5 1 E - 0 3 5 5 8 5 F - C 4 . 7 7 6 F - 0 3 6 2 9 3 F - C 4 . 4 1 5 E - C 3 4 0 2 5 E - C 4 • 7 9 I E —0 3 4 6 5 2 E - C 4 . 1 4 6 E - 0 3 3 5 7 7 E - C 4 . 8 4 IE —0 4 1 6 4 0 E - C 4 • C 9 8 E - 0 3 3 4 9 7 F - 0 4 . 7 C 8 E - 0 3 4 5 1 3 E -C 4 . 9 1 0 E -O 3 4 8 6 3 E - C 4 . 3 3 7 E - 0 3 2 2 2 8 F - C 4 • 5 6 7 E - 0 3 4 2 6 2 E - C 4 • 0 5 ° F - 0 3 3 4 3 1 F - C 4 • 7 5 C E - 0 3 6 2 5 0 F - C 4 . 3 2 3E -C 3 5 5 3 8 F - C 4 • 1 0 1 E - 0 3 3 5 C 2 F - C 4 • 8 5 3 F —0 3 3 0 8 P F - L 4 • 9 1 6 E - C 3 3 1 9 3F.-04 1 9 9 5 1 3 9 9 1 9 3 3 2 3 2 3 3 3 2 2 3 2 2 4 3 3 3 3 3 2 2 1 2 3 3 2 2 2 9 2 2 2 1 2 2 3 3 2 1 1 O 3s0«4<040<C44as aaaaaaaa ^ s-g■ > 4 NN>4 • g -jaaaa aa a aaammmamm m m mm n Ojls am t > U iu«.o lO O D am * u rv >* - otss am *U N— o<ca am * < ^ i r »**o«oa am o z noon ooooooooooC.Onoo OO O O O OO ooo o o o o o o o o o o o o o o o o o o o o o o i i i i 1 1 • 11 1 1 i iii ii1i •i ii i i ii i•i i i1ii i1 1i 1i i1ii1 11 1 S’ a ^ a m a 'jmmam *a aaa amm aa* u* ► au» Uam* ' J m **-**a m 1aUN m ■ s NU mu S40® ■ > i u ai*90» i\>aaa— aau <oaNJ OfUON asaa N »a cuNN m*»N o*NX — i m Z • • • • • • • • • • •• ••• •••• •• •• • • •• • •• • •••• • • ••• •• •••• • •• •• r> <CO'JISOUOffwarnmu a*a uN>0*“urn!fN c — -oa•Xmao NaUCD< f “C***a■ONm *Uua w. ** r o* *-gOUM» aa^j*a*<o*u aa i— N a19» aa h * l » U*“■oU < 0uC < 0aN * * * 4ua N * n u » a a - 4 * m m '4 '4 u a u o B a » * m N * - a ® U '4 m m u m N m m m u u » - u N * * u — m»* ■* * o •* * *-x -«4a«40®N*aouoroua*'04mua**aNN®N*mmNNOu'0®N*aN*'*muua** m • • • • « • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • ■ • * • • • • • • • • • • • • • ,o iON«0'^oa»euoNaauN~4u.a*''4*xum*NN.ou*am.-a4Ma'j*-***-'CmO''4uNm>oo r »oo»»ufoiru^»u| \)o>'y)a(>»o»M\)< >iii au<oiiiiuo»)y)'4'goo>u)9iuiQ!Wuosi\)n»vi(B')ix CUOly)U)«»**<JtOM**9'‘»*‘OggOI«IU'4>*U'*»-*‘U|SNVlCMNUOU*‘0»OUNOIUUI9»r3 0 D }UUa»OUimu(00»OOU4)^9^>*OOU O^UIUOOUIN OolOOO^OU?— OSM^^OUI*-^ OUIt09UI'0MI\)>*N'JIOMU^UINUN<gU)0DUIUI\)'0»O'*0'NUl»S0'N9 9i0**SSSSXMU(CUO -nm rTirnmfni-iirT'mrn ^ m m m n im r^rT irn m rT ir7 n im -"n irn n r,'m -n rn rn ^n rn m m m m T i'n -n rn m rnm -nrnrT ’ nim i i I i I i i I i I I I i I i i i i i t I I i I i i i i i i i i i i i I i i i i i i i i i i i I i i • o o o o o o o n o n o o o o o o o o o o o o o o o o o o o o o o o o o o o o o a o o o o o o o o o o o Muuuu>uuuUMUUMUuuuuwuuuuiyiii<iuwiiiiiiUuw>uiiiiii»«wuiuu juuuuuu • > N u u N X N U N * u u N * » u u u * a u m a m m u '‘ u m a a u u N N S u N » * > '4 * ~ N N N U N * ~ N N u * ' • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • ■ • • • • • • A •gl\|O0gji»»U) j)O?'JISO9Ui»S0<NUUUU'JIS J'U inw slv> *O lii» u 0 D » U '4 « *O 9 X I> 3 U N O » omuc** • j a M a i * 0 ' j o w ' i » o i ( « * o * ( j i u o ,ji d j o o 'O M aia , ji? - u u o u ir e -j^ M N -g o u u a fo s smmo*-*- —> 4 m u m o a N a '0 '4 a u m » © '0 *u a *-o N ^ u rx>'4N O 'jo.-om o*N»0'0***4**-u u nmrrmnir!i"nrTir,!mrT'rn''n'nninirnmmmmrn'T!rT'Ti"nrnnimninmmi'n''*mn',i rn''nfnrri ' , fnmTirn"T i o : o o '’’ I i I I i i I i i i i i i I I l i I I i i I i i i I i i I i i i i i i I I i I i l l I I I i l I I i I o o o o a o o o o o o o o o a o o < ~ > o n r > o o o n ' ' f > o 3 i o f ' ^ o o o ' i o f l c o n o n o o o n n n n ro O 205 CM IN C L DECL M J IC 10 - 7 3 . 4 1 1 8 . 4 1 1 . 3 9 5 E - C J 2 . 3 2 5 E - 0 4 1020 - 2 . 5 4 2 . 5 4 9 . 4 2 4 E —0 3 1 . 5 7 1 L - C 3 1 0 3 0 - 8 3 . 8 5 5 6 . 2 5 7 . 1 4 6 E - 0 4 1 . 1 9 1 E —C 4 1040 - 4 9 . 9 3 3 2 . 16 2 . C 7 4 E - C 3 3 . 4 5 7 E - 0 4 1 0 5 0 - 4 4 . 0 8 7 5 . 8 8 3 . 6 0 2 E - C 3 6 . 0 C 3 F - C 4 10 6 0 - 6 7 . 0 5 6 3 . 3 6 1 . 2 0 2 E - 0 3 2 . 0 C 4 E - 0 4 10 7C - 5 3 . 6 0 4 6 . 4 2 1 . 9 4 6 ^ - 0 3 3 . 2 4 3 E - C 4 1 0 8 0 - 2 5 . 0 2 8 3 . 2 0 2 . 3 6 9 E - C 3 3 . 9 4 9 E - 0 4 109C - 4 7 . 1 4 5 9 . 6 8 2 . 5 6 4 E - 0 3 4 . 2 7 3 0 - 0 4 1 1 cc - 5 4 . 6 4 70 . 2 7 1 . C 7 5 E - C 3 1 . 7 9 2 E - 6 4 1 1 1 0 - 4 8 . 1 5 4 9 . 9 9 1 . 5 1 4 E - 0 3 2 . 5 2 3 E - 0 4 11 2 0 - 2 8 . 4 2 6 5 . 10 5 . 2 6 5 E - 0 1 8 . 7 7 4 E -C 4 . 3 9 - 2 4 DEMAG SAMPLS 2 C 0 -2 5 C OE CM IN C L DECL M J 34 0 - 4 5 . 6 6 6 9 . 9 4 2 . 1 C 2 E - 0 3 3 . 3 0 3 E - C 4 55C - 2 3 . 5 4 S 0 . 6 S 4.8 6 1 E - 0 4 8 . 1 0 2 E - C 5 5 8 0 - 6 0 . 6 0 2 6 . 5 4 8 . 1 0 8 E - 0 4 I • 3 5 1 L —C 4 6 2 0 - 4 6 . 4 9 4 4 . 10 4 . 3 1 9 F - 0 4 7 . 1 9 8 E - 0 5 6 7 0 - 1 6 . 4 6 4 8 . 7 1 7 . 7 3 8 E - 0 4 1 . 2 9 0 E - C 4 950 - 7 4 . 3 9 3 6 . 8 3 7 . 8 0 9 E - 0 4 1 . 3 0 I E - 0 4 £ 1 9 - 2 4 TRIGGER CORE NRM CM IN C L DECL M C - 4 5 . 0 3 5 7 . 1 1 30 3 8 . 7 5 6 9 . 1 2 3 . 2 7 6 E —04 8 . 1 9 0 E - C 5 1«j434E-03 3 . 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B 9 8 F - C 4 4 7 4 4 E - C 5 70 - 8 1 58 66 73 3 . 2 9 5 E - C 4 8 2 3 8 F - C 5 80 - 6 9 28 77 82 8 . 4 8 7 6 - 0 5 2 1 2 P F - 0 S 90 - 5 8 51 53 41 1 . 3 4 7 E - 0 4 3 36S f"-C 5 100 - 5 6 64 58 61 1 . 0 2 5 6 - 0 4 2 5 6 3 F - 0 5 1 10 — 6 1 21 64 02 1 . 6 9 2 E - C 4 4 2 3 0 E - C 5 1 2C - 6 2 6 8 70 4 8 8 . 2 2 8 6 —C5 2 0 5 7 F - C 5 1 30 - 5 6 4 7 57 6 6 8 . 5 1 8 E - C 5 2 1 2 9 E -C 5 1 40 - 5 9 73 68 12 8 . 9 4 8 6 - 0 5 2 2 3 7 6 - C 5 150 - 6 4 39 64 5 8 1 . 0 1 9 E - 0 4 2 54 8 E -C 5 160 - 4 7 1 8 41 30 1 . 0 2 5 6 - 0 4 2 5 6 2 6 - 0 5 1 70 - 4 9 52 46 0 3 1 . 2 0 8 E - 0 4 3 0 2 0 6 - 0 5 1 8C - 6 1 50 52 71 1 . 3 7 8 6 - 0 4 3 4 4 6 6 - 0 5 1 9C - 6 4 6 9 15 36 2 . 9 3 3 E - 0 4 5 0 8 J E - 0 5 200 - 6 5 J5 30 9 3 3 . 5 1 6 E - 0 4 8 7 9 1 E - 0 5 2 1C - 5 2 9 5 43 55 6 . 0 4 4 E - 0 4 1 51 1E -C 4 22C - 5 6 6 9 33 65 4 . 1 2 3 6 - 0 4 1 0 3 1E -C 4 2 3C - 5 2 24 5 7C 6 . 8 6 8 E - C 5 1 7 1 7 6 - 0 6 2 4 0 — 6 6 4 7 1 1 3C 1 . 0 7 1 6 - 0 4 2 6 7 7 E -C 5 25C - 6 4 33 2 6 54 6 . 4 8 9 E - C 5 1 6 2 2 E - 0 5 2 6 0 - 5 2 16 47 44 1 . 1 1 1 E - 0 4 2 7 7 7 E - C 5 2 70 - 5 5 56 27 27 1 . 2 9 1 6 - 0 4 3 2 2 9 E - 0 5 2 «0 - 4 5 17 3C 77 1 . 7 9 6 6 - 0 4 4 4 906 —C 5 2 9 0 - 4 6 50 2 5 74 9 . 7 8 7 6 - 0 5 2 4 4 7 E - C 5 300 - 6 1 6 3 21 78 7 . 1 2 1 6 - 0 5 1 7 8 0 6 - 0 5 3 1 C - 7 5 15 18 41 1 . 0 3 7 E - O 4 2 5 9 4 E - C 5 3 2 0 - 6 1 96 14 73 8 . 7 5 6 6 - 0 5 2 18 9 E - 0 5 33 0 - 5 9 66 38 1 1 1 . 4 7 6 6 - 0 4 3 6 9 1 6 - C 5 340 - 5 7 23 20 83 8 . 6 9 3 E - G 5 2 17 3 6 - 0 5 3 50 - 5 5 60 2 5 17 1 • 3 9 2 E - 0 4 3 4 8 0 6 - 0 5 36C - 4 7 95 38 32 9 . 5 6 2 6 - 0 5 2 3 9 C 6 -C 5 3 7C - 5 9 64 44 95 1 . 1 1 3 E - 0 4 2 7 8 46 — 0 5 380 - 6 4 4 7 2 3 1 7 7 . 4 C 7 F —05 1 8 5 2 F - C 5 3 90 - 6 1 6 6 14 02 5 . 4 5 8 6 - 0 5 1 J 6 5 F - C 5 4C0 - 6 8 27 10 61 9 . 2 2 C E -G 5 2 3 C 5 6 -C 5 4 1 0 - 5 9 76 16 24 1 • C 4 C E -0 4 2 5 9 9 6 - 0 5 4 2 0 - 6 5 40 10 29 3 . 3 7 7 6 - 0 4 8 4 4 3 E - C 5 4 3 0 - 6 3 2 8 1 7 63 3 . 2 2 7 E - 0 4 8 4 0 0 - 5 7 36 26 54 1 . 5 6 2 6 - 0 4 3 9G b C -:< 5 45 0 - 6 3 76 to 77 2 . 0 2 6 6 - 0 4 5 0 6 - C 5 4 6 0 - 7 1 1 1 5 70 1 . 3 0 3 E - 0 4 3 257F .-C 5 4 70 - 5 9 94 4 96 9 . 6 5 3 F - C 5 2 4 1 3 6 - 0 5 4 8 0 - 5 9 76 5 19 9 . 1 8 6 6 - 0 5 2 2 9 7 E -C 5 49 0 - 5 9 56 84 4 7 8 . 7 2 1 6 - 0 5 2 1 8 0 E - 0 5 209 CM IN C L DECL M J 50C - 6 1 . 9 1 4 9 . 7 1 7 . 5 7 6 F - 0 5 1 . 8 9 4 F - 0 S 51 0 - 4 5 . 7 6 7 9 . 61 6 . 7 0 4 E - 0 5 1 • 6 7 6 E - 0 5 5 2 0 - 4 3 . 8 1 4 7 . 2 4 1 . 0 2 6 E - 0 4 2 • 5 6 4 E - C 5 5 3 0 - 5 6 . OC 3 C . 9 3 6 . 5 4 9 E - 0 5 1 . 6 3 7 E - D 5 5 4 0 - 4 1 . 7 6 1 0 . 2 9 1 • 8 8 1 E—05 4 . 7 0 2 E —06 E 3 9 - 4 ? DEMAG SAMPLS 8 0 - 1 2 5 OE CM IN C L DECL M J 50 - 8 0 . 1 3 4 4 . 9 5 8 . 6 9 5 E - C 5 2 . 1 7 4 E - C 5 2 3 0 - 5 3 . 7 0 2 9 . 7 1 5 . 7 C 1 E - 0 5 1 • 4 2 5 E - C 5 2UC - 5 7 . 1 6 3 7 . 2 6 1 . 0 1 9 E - C 4 2 . 5 4 8 F - 0 5 3 5 0 - 5 0 . 5 8 4 . 2 3 8 . 9 2 1 E - 0 5 2 . 2 J 0 E - C 5 5 4 0 - 3 8 . 2 2 3 4 . 2 5 2 . 1 2 6 E - 0 5 5 . 3 1 6 E - 0 6 210 E 3 9 - 4 4 4 7 2 6 S 1 3 4 C2 E 4 1 3 2 M NBM CM IN C L DECL M J 0 - 7 5 77 7 * 12 2 . 0 6 9 E - 0 4 5 1 7 3 F - C 5 10 - 6 6 53 3 3 * 6 5 1 . 7 0 B E - 0 4 4 2 7 0 F - 0 5 20 - 1 4 29 6 4 . 13 1 . 4 3 7 E - 0 4 3 5 9 3 F - C 5 30 - 3 8 19 2 3 . 17 4 . C 5 3 F - C 5 1 J 1 3 E - 0 5 40 - 4 1 7 6 6 3 . 3 6 4 . 5 1 4 E - 0 5 1 1 2 9 E - 0 5 5C - 5 3 29 1 8 . 41 5 . 3 1 4 E - 0 4 1 3 2 9 E - C 4 60 - 7 1 4 3 41 . 5 9 2 . 3 8 0 E - 0 4 5 9 5 C F - 0 5 70 - 6 0 18 1 6 . 3 7 2 . 2 3 9 E - C 4 5 5 9 7 F - 0 5 BO - 4 9 78 2 1 . 0 1 2 . 7 C 8 E - 0 4 6 7 6 9 F - 0 5 90 - 5 9 09 4 4 * 9 5 _ 3 . 2 B 6 E - 0 4 8 2 1 6 E - 0 5 100 - 5 8 97 5 3 . 0 7 1 . 8 2 8 5 - 0 4 4 5 7 0 E - C 5 n o - 6 0 H2 51 . 2 8 1 . 6 5 1 5 - 0 4 4 1 2 6 E - C 5 120 - 6 3 91 8 2 . 3 1 2 . 1 6 3 E - 0 4 5 4 C 7 F - 0 5 130 - 6 4 2 8 80 . 4 5 _ 2 . 6 4 3 E - 0 4 6 6 O 0 E -O 5 1 40 - 4 9 61 4 7 . 0 7 3 . 7 0 1 E—0 4 9 2 5 4 E - 0 5 1 50 - 5 9 36 5 7 . 7 4 3 . 9 3 3 E —0 4 9 8 3 2 E - 0 5 160 - 6 0 09 2 9 . 3 3 4 . 6 2 6 E - 0 4 1 I S 7 E - C 4 1 70 - 6 0 63 7 2 . 3 9 5» 1 Q 5 E -Q 4 1 2 7 6 E - 0 4 180 - 5 2 08 6 5 . 48 2 . 5 1 4 F - 0 4 6 2 8 6 F - 0 5 1 90 - 5 1 61 71 . 4 9 2 . 5 5 8 E - 0 4 6 3 9 4 E - C 5 2 0 0 - 6 0 31 3 9 . 2 5 3 . 6 0 6 E —04 9 0 1 6 E - 0 5 2 1 0 - 7 6 10 5 6 . 2 5 2 . 8 4 1 E - 0 4 7 10 2 E - C 5 2 2 0 - 6 9 23 3 5 . 9 9 2 . 4 1 31 - 0 4 6 0 3 2 E - 0 5 2 3 0 - 2 6 19 6 5 . 3 0 1 . 8 4 5 E - 0 4 4 6 1 3 F - C 5 240 - 2 8 6 3 6 3 . 3 6 1 . 4 3 8 E - 0 4 3 5 9 5 E - C 5 2 5 0 - 5 2 90 8 3 . 5 7 1 . 8 8 5 E - 0 4 4 7 1 3 E -C 5 2 60 - 4 8 78 6 2 . 0 3 3 . 6 6 5 E - 0 4 9 16 1 F - 0 5 27 0 - 5 8 5 6 7 9 . 6 1 4 . 0 3 9E — 0 4 1 0 1 O E -O 4 2 8 0 - 5 3 54 7 9 . 1 3 2 . 2 5 9 E - 0 4 5 64 7 E -C 5 2 9 0 - 5 5 26 7 4 . 0 9 1 . 3 7 2 E - 0 4 3 4 3 1 E - C 5 3 00 - 5 4 83 8 4 . 4 7 7 . 6 6 5 E - 0 5 1 9 1 6 F - 0 5 3 10 - 6 7 84 2 7 . 2 7 1 . 9 4 0 E - 0 4 4 9 4 9 E - 0 5 32 0 - 5 9 66 1 1 . 7 6 3 . 0 4 9 E - 0 4 7 6 2 3 F - 0 5 3 30 - 7 3 59 5 0 . 1 4 5 . 2 2 7 E —04 1 3 C 7 E - 0 4 34 0 - 7 3 60 4 9 . 3 4 4 . 1 1 6 E - 0 4 1 0 2 9 E - 0 4 350 - 4 3 89 51 . 5 8 5 . 3 3 I E - 0 4 1 33 3 F - 0 4 36 0 - 3 8 17 4 6 . 2 5 4 . 9 6 7 E - 0 4 1 2 4 2 E - 0 4 37C - 5 2 16 6 1 . 0 1 4 . 4 4 3 E - 0 4 1 1 1 1 E - 0 4 38C - 4 8 56 6 8 . 12 4 . 5 9 6 E —0 4 1 1 4 9 E - C 4 3 9 0 - 5 1 07 6 0 . 19 4 . 0 2 7 E —0 4 1 0 0 7 E - 0 4 4 0 0 - 5 4 6 7 6 0 . 19 4 . 3 7 7 E —04 1 0 9 4 E - C 4 4 1 0 - 3 7 21 5 8 .2 . 6 4 . J 5 0 E —04 1 0 8 8 E - C 4 4 2 0 - 3 5 64 6 3 . 78 4 . 7 3 0 E - 0 4 I 1 8 2 F - 0 4 4 3 0 - 4 1 0 6 5 3 . 3 9 6 . 0 0 8 E - 0 4 1 5 C 2 E -C 4 4 4 0 - 1 5 95 2 4 . 0 9 4 . 7 8 7 E —0 4 1 1 9 7 E - 0 4 45C - 9 43 7 8 . 19 3 . . 4 4 1 E - 0 4 8 6 0 I E - 0 5 4 60 - 4 6 0 7 7 4 . 2 7 2 . 3 4 9 E - 0 4 5 8 7 1 E - 0 5 4 70 - 3 9 4 5 3 4 . 4 7 1 . 5 7 7 F - 0 4 3 9 4 4 E - C 5 4 8 0 - 5 3 61 6 7 . 5 4 1 . 9 4 6 E - 0 4 4 8 6 4 E - C 5 4 9 0 - 5 8 21 7 2 . 8 2 1 . 6 2 2 E - 0 4 4 0 5 4 E - C 5 211 CM IN C L OECL 5 0 0 - 5 8 . 4 ? 7 6 . 8 2 1 . 7 6 5 E - G 4 4 . 4 1 3 E - C 5 5 1 0 - 6 2 . 7 7 B C . 9 4 1 . 7 6 ? E - C 4 4 . 4 0 4 E - C 5 5 2 0 - 3 5 . 7 9 4 3 . 7 3 8 . 5 6 9 E - 0 5 2 . I 4 2 E - C 5 5 3 0 - 5 7 . 2 5 4 8 . 9 4 2 . 3 5 9 E - 0 4 5 . 8 9 8 E - 0 5 E 3 9 —4 4 1ST DE MAG SAMPLS 1 0 0 - 3 0 0 OF CM IN C L DECL M 20 - 1 4 . 1 4 7 9 . 2 0 1 . 6 2 3 E - 0 4 4 • 0 5 8 F - 0 5 40 - 2 3 . 2 4 7 9 . 2 9 7 . 4 0 7 E —0 5 1 • 8 5 2 E - C 5 50 - 5 7 . 8 9 2 0 . 3 0 2 . 2 6 8 E - 0 4 5 • 8 7 1 E - 0 5 80 - 5 2 . 2 0 1 2 . C 8 9 . 7 7 8 E - C 5 2 • 4 4 5 F - 0 5 1 40 - 6 2 . 5 5 21 . 7 8 1 . 2 2 4 E - C 4 3 • 0 6 C E - 0 5 2 3 0 - 7 4 . 3 0 2 6 . 5 4 5 . 2 C 8 E - 0 5 1 • J 0 2 E - C 5 32 0 - 4 1 . 4 3 8 2 . 2 1 1 . C 4 1 E - 0 4 2 • 6 0 4 E - C 5 3 6 0 - 5 3 . 3 3 11 . 7 6 8 . 5 9 2 E —0 5 2 • 1 4 8 E - 0 5 3 9 0 - 5 8 . 7 9 1 0 . 2 9 9 . 0 3 5 F - 0 5 2 • 2 5 9 E - C 5 4 0 0 - 7 4 . 5 1 7 8 . 6 0 8 . 0 2 IE —0 5 2 • 0 0 5 E - C 5 4 1 0 - 2 2 . 0 5 8 6 . 3 3 7 . 2 3 1 E - 0 5 1 . 3 0 8 E - C 5 4 2 0 - 3 5 . 6 9 4 5 . 9 5 1 . 0 3 8 E - C 4 2 • 5 9 5 E - G 5 4 3 0 5 7 . 7 7 5 7 . 9 3 7 . 4 0 7 E - 0 5 1 • 8 5 2 E - C 5 4 4 0 4 5 . 9 0 8 2 . 7 8 7 . 2 7 0 E —0 5 1 . 8 1 B E - 0 5 4 5 0 2 2 . 9 6 81 . 7 8 1 • 605E —0 4 4 . 0 1 3 E - 0 5 4 6 0 - 2 2 . 3 2 71 . 4 9 7 . 1 4 6 E - 0 5 1 • 7 8 6 F - 0 5 4 70 1 . 5 1 3 5 . 3 2 7 . 9 4 7 E - 0 5 1 . 9 8 7 E - C 5 5 1 0 - 1 4 . 1 4 5 6 . 2 5 8 . 5 4 9 E - 0 5 2 • 1 3 7E — C 5 5 2 0 7 3 . 0 2 4 8 . 7 6 2 . 2 9 3 E - 0 5 5 • 7 3 4 E - C 6 53C 2 3 . 5 9 8 8 . 11 7 . 3 0 3 E - 0 5 1 . 8 2 6 E - C 5 E3<>-44 2ND OF MAG SAMPLS 2 0 0 - 3 0 0 OE CM IN C L OECL M 2 3 0 - 5 3 . 1 7 4 1 . 9 4 4 . 6 9 7 F - 0 5 1 . 1 7 4 E - 0 5 4 7 0 - 0 . 6 5 5 5 . 1 6 5 . 4 9 7 E - 0 S 1 . 3 7 4 E - C 5 £ 3 9 - 4 4 TRIGGER CORE NRM CM IN C L DECL M J 30 - 5 5 . 1 8 3 1 . 5 7 3 . 3 5 8 E - 0 4 8 . 3 9 5 E - 0 5 212 E 3 9 - 4 8 45 4 9 S 136 4 8 E 4 3 5 2 M NRM CM IN C L OECi_ -M J 140 - 1 8 33 7 7 . 14 6 . 5 7 1 F - 0 4 1 0 9 5 F - C 4 150 - 2 9 8 3 39-* 13 8 . 3 9 4 E - 0 4 1 3 9 9 E - C 4 160 - 3 3 18 3 9 . 0 5 1 . 0 3 0 E - 0 3 1 7 1 7 ^ - 0 4 1 70 - 1 7 75 8 3 . 4 7 1 . 3 6 9 E - C 1 2 2 8 2 E - C 4 180 - 4 0 97 71 . 4 9 2 . 1 0 2 E - 0 4 3 5 C 3 E - C 5 190 - 4 7 15 5 3 . 0 7 4 . 6 1 4 E - 0 4 . .7 6 9 1 E - C 5 2 0 0 - 2 8 73 3 . 8 1 4 . 3 0 I F — 0 4 7 1 6 8 E - 0 5 2 1 0 - 1 8 72 8 2 . 4 1 8 . 4 5 9 E —0 5 1 4 1 0 E - C 5 2 2 0 - 4 8 25 1 2 . 0 2 1 . 9 5 9 E - 0 4 3 2 6 6 E —0 5 2 3 0 - 8 0 75 7 . 1 2 3 . 1 7 5 E - Q A . 5 2 9 2 E - 0 5 2 4 0 - 5 2 97 6 8 . 8 9 5 . 8 0 8 F - 0 4 9 6 8 0 E - 0 5 2 5 0 - 3 78 7 0 . 5 9 1 . 2 6 S E - 0 4 2 1 C 9 E - 0 5 26C - 2 6 60 6 8 • 1 > 1 . 2 5 9 E - 0 3 2 0 9 8 F - C 4 2 7 0 4 36 82 *-89 L . 3 7 3 E - 0 3 2 2 8 8 E - C 4 2 8 0 - 3 2 6 5 8 5 . 0 6 1 . 4 7 0 E - 0 3 2 4 5 I E —0 4 2 9 0 - 4 8 39 5 5 . 6 1 1 . S 6 4 E - 0 3 2 6 0 7 E - 0 4 3 0 0 42 57 2 8 . 7 8 1 . 2 9 6 E - 0 3 2 16 I E —0 4 3 1 C - 2 7 4 6 7 6 . 8 1 1 . 7 6 6 E - 0 3 2 9 4 3 E —04 3 2 0 - 5 7 35 8 4 . 4 7 2 . 4 5 6 E - C 4 4 0 9 3 E - 0 6 3 3 0 - 4 4 21 3 6 . 3 4 2 . 0 6 6 E - 0 4 3 4 4 4 E - 0 5 3 4 0 - 4 8 10 4 4 . 9 5 2 . S 2 S E - C 4 4 2 0 9 E - C 5 35C - 3 6 5 2 3 6 . 3 4 3 . 6 8 4 E - 0 4 6 1 4 1 E - 0 5 3 6 0 - 2 0 6 5 8 7 . 3 6 1 . 0 0 6 E - 0 3 1 6 7 7 E - 0 4 3 7 0 40 27 4 4 . 9 5 9 . 6 9 1 E - 0 4 1 6 1 5 F - C 4 3 8 0 - 1 37 2 4 . 0 8 8 . 7 0 3 E - 0 4 1 4 5 1 E - 0 4 3 9 0 - 2 2 71 7 3 . 70 1 . 2 9 8 E - 0 3 2 1 6 3 E - 0 4 4 0 0 - 8 0 8 1 6 . 4 9 1 . 1 8 9 E - 0 3 1 9 8 2 E - C 4 4 1 0 - 5 4 15 8 3 . 9 0 4 . 0 9 7 E - 0 4 6 8 2 8 E - 0 5 4 2 0 2 7 8 3 6 3 . 3 6 1 . 1 6 3 E - 0 3 1 9 3 8 E - C 4 4 3 0 3 C2 4 7 . 6 2 . 1 , 5 6 5 3 - 0 3 - 2 6 4 2 E - C 4 4 4 0 3 5 8 2 51 . 6 5 1 . 2 4 9 E - 0 3 2 0 8 I E —0 4 4 5 0 - 5 1 5 8 41 . 9 4 4 . 0 7 8 8 - 0 4 6 7 9 7 E - C 5 4 6 0 - 2 9 13 7 7 . 5 2 6 . 6 9 0 E - 0 4 1 1 1 5 E - C 4 4 70 2 2 32 8 6 . 54 - 7 . 6 9 6 E - C 4 1 2 8 3 E - C 4 4 8 0 - 3 2 2 3 6 0 . 8 8 5 . 0 8 9 E - C 4 8 4 8 2 E - C 5 4 9 0 - 5 7 01 7 2 . 8 2 3 . 1 38F —0 4 5 2 2 9 E - 0 5 5 0 0 - 4 9 43 2 9 . 8 7 1 . 4 8 4 E - C 4 2 4 7 4 E - C 5 5 1 0 - 2 2 71 6 5 . 1 5 6 , 4 8 9 E - 0 4 1 0 8 2 E - C 4 5 2 0 - 6 0 5 8 5 7 . 0 3 2 . 5 9 0 E - 0 4 4 3 1 6 E - 0 5 5 3 0 - 3 5 0 6 7 8 . 6 0 4 . 6 8 9 E —0 4 7 8 1 5 E - 0 5 5 4 0 - 4 0 6 3 4 6 . 0 7 8 . 9 4 6 E - 0 4 1 4 9 I E —0 4 5 5 0 15 32 6 7 . 20 _L*Z39JE-03 2 8 9 8 E - 0 4 5 6 0 19 43 8 4 . 3 8 1 • 3 8 1 E - 0 3 2 3 0 1 E - C 4 5 7 0 - 4 0 81 71 . 0 0 3 . 0 6 7 E - 0 4 5 1 1 2 E - 0 5 5 8 0 - 4 0 97 2 9 . 5 4 3 . 5 3 5 E - 0 4 5 8 9 2 E - 0 5 5 9 0 - 7 6 10 4 4 , 9 5 2..930E-JD4 4 9 5 C E - C 5 61 0 - 5 2 01 6 6 . 9 4 3 . 6 5 7 E - 0 4 6 0 9 4 E - 0 5 6 2 0 - 4 4 2 6 7 7 . 3 8 5 . 6 5 5 E - 0 4 9 4 2 5 E - 0 5 6 3 0 - 2 2 6 2 2 9 . 3 6 5 . 5 3 6 E - 0 4 9 2 2 7 E - 0 5 6 4 0 - 7 2 84 1 2 * 3 1 — 5 * 9 0 3 E - 0 4 9 8 3 9 E - 0 5 213 CM IN C L DECL M J 65C - 1 1 . 1 3 6 4 . 88 6 . 4 9 0 F - 9 4 1 . 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A C 2 . 6 3 3 F - 0 A A . 3 8 8 E - 0 5 3A0 —A A . 1 3 3 0 . 9 3 1 . 0 2 0 E - O A I . 6 9 9 E - 0 5 216 3 9 - 5 C 47 0 7 S 142 31 E 4 4 4 3 M NWM CM IN C L DECL M J 0 - 4 5 85 2 6 54 5 . 2 3 8 E - 0 4 1 3 1 9 5 - 0 4 10 - 4 1 92 2 9 9 5 5 . 0 6 3 E - 0 4 1 2 6 6 F - 0 4 20 - 4 5 76 23 36 7 . 2 5 5 E - 0 4 1 8 1 4 E -C 4 30 - 3 9 56 29 9 8 4 . 2 2 9 E - 0 4 1 0 5 7 1 - C 4 40 - 8 2 04 9 4 5 2 . 7 8 5 E - 0 4 6 9 6 3 E - C 5 5C - 5 2 30 18 41 3 . 2 4 7 E - 0 4 8 1 1 6 E -C 5 60 - 4 5 95 33 6 5 4 . 8 8 l b - 0 4 1 2 2 0 E - 04 70 - 4 0 0 6 4 4 31 5 . 1 5 9 E - 0 4 1 2 9 0 F - C 4 80 - 5 5 1 7 30 9 3 3 . 2 0 6 E - 0 4 8 0 1 4 E - 0 5 90 - 5 2 42 18 04 4 . 9 8 1 E - C 4 1 2 4 5 E - C 4 ICO - 5 3 38 8 61 3 . 5 1 3 E - 0 4 8 7 8 2 E - 0 5 1 10 - 5 3 27 17 91 3 . 7 5 2 E - 0 4 9 3H C E -G 5 1 20 - 7 4 70 44 9 5 5 . C 6 8 E - 0 4 1 2 6 7 E - C 4 1 30 - 5 2 30 11 62 3 . 5 6 3 E - 0 4 9 9 C 9 E - 0 6 1 40 - 4 8 84 13 80 5 . 9 9 I E - 0 4 1 4 9 8 E - C 4 150 - 6 5 40 a 12 7 . 1 2 1 E - 0 4 1 7 R 0 F -C 4 1 60 - 4 7 9 2 50 14 7 . 3 1 5 F - 0 4 1 8 2 9 E - 0 4 1 70 - 5 2 32 54 72 7 , 1 2 4 E - 0 4 1 7 8 1 E - C 4 1 80 - 7 5 97 31 9 7 8 . 1 8 3 F - 0 4 2 0 4 6 F - C 4 1 90 -<•7 1 7 9 4 5 6 . 5 7 3 E —04 1 6 4 3 E - 0 4 ?co - 5 4 4 7 8 96 6 . 9 2 9 E - 0 4 1 7 3 2 E - 0 4 2 1 0 - 6 6 C8 8 12 7 . 3 1 2 E - 0 4 1 8 2 0 E - C 4 2 2 0 - 6 7 04 39 7 6 5 . 0 3 6 E - 0 4 1 2 5 9 E - C 4 2 3 0 - 4 9 33 31 9 7 3 . 6 3 4 E - 0 4 9 0 8 6 E - C 5 2 4 0 - 5 5 84 18 8 3 4 . 8 4 6 E - 0 4 1 21 I E - 0 4 2 5 0 - 5 5 5 8 12 79 8 . 3 5 5 E - 0 4 2 0 B 9 E - 0 4 2 6 0 - 7 1 61 35 5C 1 . 1 4 5 E - C 3 2 0 6 2 f - C 4 2 70 - 7 7 83 15 93 7 . 2 6 7 E - C 4 1 0 1 7 5 - 0 4 2 8 0 - 5 8 97 15 24 9 . 2 6 2 E - 0 4 2 3 1 6 6 - 0 4 2 9 0 - 6 6 60 14 91 8 . 1 9 4 F - C 4 2 O 4 0 E -O 4 3 0 0 - 3 7 10 6 7 24 5 . 7 1 2 E - 0 4 1 4 2 8 E - 0 4 310 - 4 0 75 62 69 6 . 3 3 4 F - 0 4 1 5 8 3 E - 0 4 3 2 0 - 4 4 15 51 0 2 5 . 8 4 6 E - 0 4 1 4 6 1 F - 0 4 33C - 3 8 6 6 79 42 7 • 3 5 4 E - C 4 1 0 3 B E -O 4 34C - 4 5 93 4 8 76 6 . 3 9 4 E - C 4 1 5 9 9 E - C 4 3 50 - 4 6 59 46 1 3 7 . 7 6 1 E - C 4 1 94CF — r 4 360 - 5 1 64 54 19 1 • 0 3 9E - 0 3 2 5 9 7 F .-0 4 3 70 - 3 3 CC 54 05 7 . C 1 6 C - C 4 1 7 5 4 E -G 4 3 80 - 5 1 61 10 41 2 . 2 3 8 E - C 4 5 5 9 5 E - 0 5 30c - 6 4 0 3 43 32 3 . 5 5 5 E - C 4 8 8 0 6 E - C 5 4 0 0 - 4 6 41 21 78 9 . 8 0 3 E - C 4 2 4 5 1E — 0 4 4 1 0 - 5 0 0 5 2 3 4 7 8 ^ 1 7 2 E - 0 4 2 0 4 3 E - 0 4 4 2 0 - 4 8 4 9 5 8 97 5 . 5 2 2 E - 0 4 1 3 0 C E -C 4 43C - 3 6 03 59 93 8 . 7 7 6 F - C 4 2 1 95 6 —C 4 4 4 0 - 5 2 50 62 2 3 1 . 5 5 3 E - 0 3 3 8 8 3 6 - 0 4 4 5 0 - 3 8 23 59 91 8 . 3 0 1 E - C 4 2 0 7 E F - C 4 46C - 3 1 60 8 8 5 5 . 7 3 9 E - 0 4 1 4 3 5 6 - 0 4 4 7 0 - 4 5 78 2 9 3 7 5 . 6 8 2 E —0 4 1 4 2 C f - C 4 4 8 0 - 5 0 83 2 2C 8 . 6 2 C E - C 4 2 1 5 5 6 - C 4 4 9C - 5 2 34 2 8 6 6 . 8 5 9 E —04 1 7 1 5 F - 0 4 217 CM INCL OECL 5 0 0 - 5 5 39 1 9 . 9 6 5 1 0 - 5 8 98 1 1 . 3 0 5 2 0 - 6 7 55 2 3 . 1 7 5 3 0 - 4 4 31 4 . 3 9 5 4 0 - 6 5 53 8 . 7 4 5 5 0 - 5 8 46 2 4 . 0 8 5 6 0 - 5 8 37 9 . 8 5 5 7 0 - 5 9 99 4 . 2 3 5 8 0 - 5 4 36 3 . 2 7 5 9 0 - 5 9 83 7 . 4 2 6 0 0 - 4 1 97 31 . 9 7 6 1 0 - 3 8 37 7 ^ 5 9 6 2 0 - 3 7 77 2 2 . 8 1 6 3 0 - 4 2 98 2 8 . 7 1 6 4 0 - 2 2 30 3 4 . 7 4 6 5 0 61 14 S 8 . 6 1 6 6 0 6 47 5 8 . 27 6 7 0 3 41 6 3 . 3 6 6 8 0 - 0 89 7 3 . 7 3 6 9 0 - 1 1 62 8 6 * 2 7 7 0 0 - 1 2 48 6 4 . 9 1 7 1 0 1 1 89 7 2 . 9 5 7 2 0 - 4 1 15 7 9 . 8 3 7 3 0 23 3 4 5 5 . 3 9 . 7 4 0 5 85 6 1 . 7 9 7 5 0 - 3 3 74 8 0 . 7 5 7 6 0 4 4 39 7 8 . 6 0 7 7 0 6 22 7 8 . 9 1 7 8 0 12 0 9 5 4 . 5 4 7 9 0 - 1 3 36 3 3 . 6 5 8 0 0 - 5 6 34 2 9 . 0 2 8 1 0 - 6 0 25 4 6 . 9 2 8 2 0 - 1 4 23 5 5 . 2 8 8 30 - 1 8 41 5 8 . 5 6 8 4 0 - 5 5 1 3 7 4 . 6 6 8 5 0 - 5 16 4 0 . 5 6 8 6 0 - 1 9 23 7 7 . 8 2 8 70 - 6 5 12 5 6 . 2 5 8 8 0 - 2 6 43 8 4 . 4 1 8 9 0 4 3 89 6 2 . 3 8 9 0 0 2 6 46 4 8 . 31 9 1 0 - 2 5 57 2 5 . 17 9 2 0 - 5 3 4 8 8 5 . 33 9 3 0 - 5 0 33 5 9 . 2 0 9 4 0 - 1 7 50 3 0 . 3 1 9 5 0 2 4 32 8 1 . 7 8 9 6 0 19 58 8 0 . 4 5 9 7 0 9 49 6 6 . 9 4 9 8 0 21 93 2 8 . 4 1 9 9 0 31 64 2 4 . 0 1 0 0 2 4 5 93 4 8 . 7 6 M J 8 . 6 2 7 E - 0 4 2 I 5 7 E - 0 4 8 . 2 8 7 E - 0 4 2 0 7 2 F - 0 4 8 . 3 6 3 E - 0 4 2 0 9 1 E - 0 4 4 . 5 7 4 E - Q 4 1 1 4 3 E - C 4 6 . 6 5 5 E - C 4 1 6 6 4 E - C 4 1 . 6 6 6 E - 0 3 4 166 E —04 9 . 3 2 I E - 0 4 2 3 3 0 F - 0 4 1 . 1 3 4 E - 0 3 2 8 3 4 E - 0 4 1 . 2 5 9 E - 0 3 3 1 4 8 6 —04 9 . 6 6 4 E - C 4 2 4 1 6 E - C 4 1 . 5 9 2 E - 0 4 3 9 8 1 E - C 5 2 . 4 2 2 E - C 4 6 0 5 5 E - C 5 3 . 2 7 2 E - 0 4 8 1 8 1 F - 0 5 6 . 0 6 5 E - 0 4 1 5 1 6 E - 0 4 2 . 9 7 I E - 0 4 7 4 2 7 E - 0 5 3 . 5 0 . 6 E - 0 4 8 7 6 4 E - 0 5 1 . 4 8 3 E - 0 4 3 7 0 7 E - 0 5 2 • I 0 7 E - 0 4 5 2 6 7 E - C 5 4 . 0 4 8 E - 0 4 1 0 1 2 E - C 4 4 . 0 4 I E - 0 4 1 0 1 C E - C 4 3 . 1 8 9 E - 0 4 7 9 7 3 E - 0 5 3 . 9 5 3 F - C 4 9 8 8 1 E —0 5 3 . 8 0 8 F - 0 4 9 5 2 1 E —0 5 1 . 6 8 6 E - C 4 4 2 1 5 E - 0 5 2 . 0 4 9 E - 0 4 5 1 2 3 E - C 5 1 • 5 7 9 E -C 4 3 9 4 8 E - 0 6 1 . 7 9 1 E - 0 4 4 4 7 8 F - 0 5 2 .3 1 3 E -C 4 5 7 8 3 F - C 5 2 . 9 8 9 E - 0 4 7 4 7 3 E - C 5 3 . 2 5 3 E - 0 4 8 1 3 3 F - 0 5 7 . 7 7 8 F - 0 4 1 9 4 5 E - 0 4 5 . 1 9 6 E -Q 4 1 2 9 9 E - 0 4 2 . 1 2 3 E -C 4 5 3 C 8 E - 0 5 2 . 1 1 6 E - 0 4 5 2 8 9 E - C 5 2 . 0 8 7 E - 0 4 5 2 1 8 L - C 5 1 . 1 6 1 E - C 4 2 9 0 2 E - C 5 6 . 3 3 9 E - 0 5 1 5 8 5 E - C 5 1 . 7 9 6 E - C 4 4 4 9 C E - 0 5 1 . 2 2 0 E - O 4 3 0 4 9 F - 0 5 7 . 5 3 C E - D 5 1 8 8 2 E - C 5 P . 4 3 5 E - C 5 2 1 0 9F.-C5 2 . 6 1 2 E - 0 4 6 5 3 1 F - C 5 3 . 0 1 4 E -C 4 7 5 3 4 E - C 5 4 . 2 3 3 E - 0 4 1 0 5 8 E - C 4 3 . 1 2 4 E - 0 4 7 B 0 9 F - C 5 2 . 4 3 3 E - 0 4 6 O 8 3 E - 0 5 2 . 4 2 9 E - 0 4 6 0 7 3 E - C 5 2 . 2 7 9 E - 0 4 5 6 9 7 E - C 5 3 . 6 9 0 E - 0 4 9 2 2 6 E - C 5 5 . 9 7 C E -7 4 1 4 9 2 E - C 4 J . 8 3 6 E - 0 4 9 5 9 1 E—0 5 co r l C V J i f . - 9 a ' - S ' ■ » U J « I f ) I T OOUUOUOOO 1 1 1 1 1 1 1 1 1 u.u.U'UidJubJUJuj r o — «oii®r>0‘i f l ' 0 ■ > O—N < 0 c ©OOCM J0®0«*»4lflN U J • •••••••• c o i n CM ooooouooo • 1 1 1 1 1 1 1 1 1 o UJUJUjU jUJUjU jUJuJ I f . 2 itPIOOxlANgo z CflACNDPin? 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J C - 2 0 91 5 2 . 19 2 . 6 3 2 E - 0 4 6 5 8 0 E - C 5 10 6 8 6 7 8 6 . 4 4 1 . 9 0 6 E - 0 4 4 7 6 5 E - 0 5 3C 4 7 92 3 3 . 6 5 4 . 5 0 2 E - C 5 1 1 2 5 F - C 5 50 - 4 8 27 8 2 . 3 1 1 . 4 2 7 E - 0 5 3 5 6 8 E - 0 6 60 - 6 0 44 4 4 . 9 5 1 . 2 0 1 E - 0 5 3 0 0 2 E - 0 6 70 - 7 1 97 3 0 . 9 3 3 . 9 5 4 E - Q 5 9 8 8 6 E - C 6 130 - 7 5 77 6 0 . 19 6 . 8 9 7 E - 0 5 1 7 2 4 E - 0 5 1 50 - 5 1 00 4 4 . 9 5 1 . 8 8 1 E - 0 5 4 7 0 2 E - C 6 1 60 50 60 2 6 . 5 4 8 . 1 0 8 E - 0 5 2 0 2 7 E - 0 5 1 7 0 44 62 8 . 7 4 3 . 8 6 5 E - C 5 9 6 6 3 E - C 6 180 63 19 7 .1 > 3 . 7 4 5 F - 0 5 9 3 6 1 E - C 6 2 1 0 19 25 4 5 . 5 9 4 . 1 8 0 E - 0 5 1 0 4 5 E - C 5 24 0 19 25 4 5 . 5 9 4 . 1 8 0 E - C 5 1 0 4 5 F - C 5 50C 73 74 6 6 . 8 9 1 .JD 4 5 E -C 4 2 81 1 E -C 5 6 3 0 6 5 86 8 4 . 2 0 1 . 0 3 0 F - 0 4 2 5 7 5 E - 0 5 6 4 0 44 56 6 3 . 9 3 4 . 0 1 8 E - 0 5 1 0 0 4 5 - 0 5 73C 40 5 7 7 7 . 5 3 3 . 4 6 7 E —0 5 8 6 6 8 E - C 6 7 6 0 54 30 5 4 . 4 0 6 . 1 7 2 E - 0 5 1 5 4 3 E - C 5 77C 6 3 91 3 9 . 7 6 7 . 4 4 2 F —0 5 1 3 6 1 F - 0 5 7 9 0 63 31 2 8 . 5 8 5 . 8 4 5 F - 0 5 1 4 6 1 E - T 5 94C 67 76 9 . 4 5 7 . 1 6 1 F - G 5 1 7 9 0 E - C 5 9 9 0 40 90 4 9 . 3 4 2-.-5S I E - 0 5 6 3 7 6 E - 0 6 1 2 0 0 40 52 2 8 . 3 6 1 . 1 5 7 E - 0 4 2 8 9 3 E - 0 5 1 210 45 35 5 9 . 4 7 1 . 7 6 1 E - 0 5 4 4 C 3 E - 0 6 12 20 50 9 7 7 3 . 9 7 2 . 1 7 7 E - 0 5 5 4 4 4 E - 0 6 1 2 9 0 40 97 ie.4i 3 • 5 0 3 E - 0 S 8 7 5 9 E - 0 6 1 3 2 0 67 8C 6 3 . 3 6 7 . 4 4 5 F —0 5 1 3 6 1 E - C 5 1 3 3 0 - 7 5 47 3 3 . 6 5 3 . 0 2 1 E —0 5 7 5 5 4 E - 0 6 1 3 4 0 - 3 0 62 5 7 . 0 3 4 . 9 1 9 E - 0 5 1 2 3 C E - 0 5 1 3 5 0 - 6 0 73 6 3 . 3 6 2 . 8 7 3 E - 0 5 7 1 8 3 E - C 6 1 3 6 0 - 3 9 33 2 4 . 2 0 5 . 9 3 0 E - 0 5 1 4 8 2 E - 0 5 E 3 9 - 5 6 2NO DEMAG SAMPLS 2 0 0 OE CM INCL DECL M - 2 2 . 8 8 5 0 . 1 4 1 . 7 7 2 F - 0 4 4 . 4 3 0 E - 0 5 E 3 9 - 5 6 TRIGGER CORE NRM CM INCL DECL 10 - 6 8 . 7 4 2 0 . 8 3 3 . 9 0 C E - C 4 9 . 7 5 C E - 0 5 E 3 9 — 5 6 TRIGGEP CORF 100 OE CM IN C L DECL 10 - 6 7 . 6 7 3 . 0 1 2 . 1 0 0 F - C 4 5 . 2 5 C E - C 5 CM IN C L OECL M J 10 10 6 7 43 10 2 9 6 1 0 8 E - 0 5 1 . 5 2 7 F - C 5 1020 5 6 27 2 6 54 1 18 0 E -C 4 2 • 95 1 E - flb 1 0 30 45 74 34 89 6 91 0 E -C 4 1 . 7 2 8 0 - 0 4 1 0 * 0 41 21 37 83 4 7 5 4 L - 0 4 1 . 1 6 9 E - C 4 10 50 4 5 84 4 3 40 2 35BF - 0 4 5 . 6 9 4 E - C 5 1 0 6 0 54 17 14 60 2 5 5 0 F - 0 4 6 • 3 7 5 E -C S 1 0 70 54 33 19 1 6 6 74 1 F -C 5 2 . 1 6 5 E - C 5 1C BO 5 0 89 31 3 9 6 9 9 8 E - 0 5 1 . T4 9 E -C 5 1 09C 5 9 4 3 20 53 7 0 3 5 F - C 5 1 • 7 B 9 t - C S 1 100 38 4 8 8 4 2C 6 0 5 4 E - 0 4 2 . 0 13 E -0 5 1 1 1 C 56 10 50 38 2 2 3 9 0 - 0 4 5 • S 9 9 F - C 5 1 1 2C 61 G 3 61 C5 1 4 3 2 E - 0 4 3 • 5 8 1 E - 0 5 1 1 30 5 5 65 77 8? 5 3 1 2 E - 0 5 1 . 3 2 8 E - 0 5 1 1 * 0 6 8 51 1 1 30 1 1 6 7 F - 0 4 2 . 9 1 9 E - 0 5 1 15C 77 1 1 5 3 0 7 4 7 1 5 E - 0 5 1 . 1 7 9 E - C 5 1 160 7 9 26 30 9 3 6 5 9 3 E - C 5 1 • 6 4 8 E - C 5 1 1 70 73 36 77 38 6 7 6 9 E - 0 5 1 • 6 9 C F -C 5 1 1 60 41 50 65 61 1 3 8 7 E - 0 4 3 • 46 6E —05 1 160 5 3 24 2 6 54 1 B 7 7 E - C 4 4 . 6 9 2 r - C 5 12 >C 35 92 39 7 6 3 6 3 0 E - C 4 9 . 0 7 5 0 - 0 5 1 210 4 9 5 8 72 62 4 3 8 9 E - C 5 1 . 0 9 7 ^ - 0 5 1220 4 4 67 2 6 54 9 2 0 8 E - 0 5 2 . 3 0 2 E - 0 5 1 230 5 2 06 4 5 6 9 1 8 G 4 E - 0 4 4 • 6 3 4 F - 0 5 124C 52 39 30 70 1 4 7 6 E - C 4 3 • 6 9 1 E - 0 5 1 2 SC 55 10 88 1 1 2 3 4 3 E - 0 4 5 . 8 5 7 ^ - 0 5 126C 2 3 94 61 78 1 1 3 2 E - 3 4 2 . 6 3 C E - C 5 1 270 53 99 87 61 1 7 8 I E - 9 4 4 . 454E - 0 5 1260 6 6 9 7 87 30 1 1B C E -C 4 2 . 9 5 1 F - C 5 1 2 9 0 - 3 2 26 21 1 4 6 21 BE- 0 5 2 • D 5 4 F - 0 5 1 300 6 8 6 6 18 41 4 3 7 3 E - 0 4 1 • 0 9 3F - C 4 1 3 1 0 61 62 62 28 1 0 4 5 E - 0 4 2 . o 1 1F.-C5 1 320 6 9 40 6C 88 3 6 8 2 E - 0 4 9 • 2 0 6 E - C 6 1 33 0 - 6 4 C9 64 73 2 01 I t - 0 4 5 . 0 9 B F - C 6 1340 - 1 7 40 78 60 3 35 IF —04 H . J77{ - C 5 1 35C - 7 92 6 8 12 2 7 2 7 E - 0 4 6 . 3 1 B F - f 5 1 3 6 0 - 3 8 22 78 14 1 9 5 8 E - 0 4 4 • 3 9 4 E - 0 5 13 70 33 64 24 01 2 C 3 5 E - 0 4 5 . 0 8 8 6 - 0 5 1 380 6 9 52 71 4 9 2 2 7 5 F - 0 4 5 • 6 H 6 E - C 5 • 3 9 - 5 8 4 8 16 S 14 7 39 F 2 3 9 5 M NRM CM INCL DECL M J 0 - 2 1 62 58 f< 7 7 3 6 6 E - 0 5 1 . 8 4 1 E -C 5 10 - 3C 60 76 3 8 1 3 505 - 04 3 • 3 7 6 E - C 5 20 - 3 2 27 70 2 1 1 7 6 C F - 0 4 4 • 4 0 C E - C 5 30 - 4 J 27 65 27 3 1V 9 F - C 4 7 . >97E - 0 5 40 - 3 4 22 87 30 1 6 7 1E — 0 4 4 . 1 7 7 E - C 5 50 - 3 9 92 78 60 1 5 2 9 E - 0 4 3 • 8 2 4 E - C 5 6C - 4 4 89 86 19 2 2 7 8 E - 0 4 5 • 6 96E — C 5 70 - I B 36 85 14 5 3C 4E-C 5 1 . 3 2 6 E -C 5 ec - 5 4 84 67 31 9 4 5 1 E - C 5 2 . 3 7 3 E -C 5 90 - 3 4 87 85 3 3 1 2 7 8 E - C 4 3 • 1 9 6 E - C 5 1 0 0 - 6 4 0 9 68 5 5 1 1 8 4 E -C 4 2 • of. i e - C 5 1 10 -6 1 53 61 95 1 5 9 2 E —04 3 • 9 8 0 5 - 0 5 1 20 - 5 9 35 6 7 31 1 0 6 8 E - 0 4 2 . 6 7 C F - 0 5 1 30 - 5 4 91 82 78 1 1 7 4 E - 0 4 2 • 9 3 5 E - C 5 1 40 - 5 2 50 83 3 9 1 21 I F - 0 4 3 • 0 2 7 E —05 I 50 - 4 8 21 40 5 6 8 6 8 3 E - C 4 2 . 1 7 1 E -C 4 1 60 - 4 6 54 53 6 9 1 6 9 7 E - 0 4 4 . 2 4 3 E - C 5 1 70 - 4 3 93 34 5 5 3 0 7 0 E - 0 4 7 • 6 7 4 E - C 5 1 00 - 7 6 50 9 4 5 1 0 9 6 E - 0 4 9 . 74CE —C 5 1 90 58 98 1 1 30 8 2 8 7 E - 0 5 2 • 0 7 2 F - C 5 ? o c 38 62 8 36 1 8 4 C E - 0 4 4 . i 9 9 E - C 6 2 1C - 4 9 1 1 44 95 4 9 7 2 E - 0 5 1 • 2 4 3E - C t> 2 20 - 5 3 70 82 7 8 5 7 0 1 E - 0 5 1 . 4 2 5 5 - 0 6 2 3C - 7 0 86 37 83 7 2 9 7 E - 0 5 1 • 0 2 4 F - C 5 2 4 0 - 7 6 74 21 78 1 4 8 1 E - 0 5 3 . 7 0 3 E -C 6 2 50 2 7 72 37 8 3 1 6 1 6 E - 0 5 4 • 0 3 9 E - 0 6 260 39 33 46 80 1 7 7 9 F - 0 5 4 • 4 4 7 8 - 0 7 2 7C 37 53 9 6 8 •» 2 9 C t —05 3 . 2 ? 6 r - C 6 200 - 6 3 3b 36 8 3 7 C 1 0 E - C 6 1 . 7 5 3 5 - 0 6 2 9 C - 1 8 91 30 93 1 2 B B E -C 5 3 . 2 2 1 E -C 6 300 - 4 1 74 6 84 4 2 3 4 5 - 3 5 1 . 0 5 9 F - 0 5 310 9 89 29 2 2 1 8 2 4 E - C 5 4 . 5 5 CE - 0 6 320 1 5 78 44 9 5 2 7 6 4 E - C 5 6 .9 1 1F.-C6 3 JO 2 9 88 32 44 1 8 8 6 E - 0 5 4 • 7 1 6 E - C 6 34 0 22 56 16 9 1 1 6 3 3 F - C 5 4 . 9 8 2 E - C 6 3 50 - 2 1 2C 33 6 5 1 21 3 5 - 0 5 3 • 3 3 1 E - C f 3 6C - 3 8 C 1 63 36 7 1 2 1 E - 0 6 1 .7 8 C E - C 6 3 70 - 2 8 75 73 9 7 1 562F - 0 5 3 . 9 0 6 5 - 0 0 3 80 - 3 3 33 4 8 76 7 9 8 0 E - 0 6 1 . 9 9 5 E - C 6 39C 1 4 45 81 2 6 3 C 1 3 E -O S 7 . 5 3 2 E - C 6 4 0 0 22 17 44 9 5 2 4 9 0 E - C 5 6 . 2 2 S E - C 6 41 0 10 38 44 9 5 2 4 3 4 E - 0 5 6 . 0 8 5 E - C 6 42C 4 C 75 25 53 2 1 1 I E - 0 5 5 . 2 7 9 E - C 6 43C 1 4 75 18 41 1 2 3 0 E - 0 5 3 •0 7 6 E - 0 6 4 4 C 27 91 44 9 5 1 6 0 6 E - C 5 4 . 0 1 5 5 - 0 6 45C 1 8 76 35 2 7 1 9 4 B E - C 5 4 . 8 6 9 5 - 0 6 4 6 r - 2 6 50 4 9 71 2 3 8 7 E - 0 5 5 • 9 6 7 E - C 6 47C 35 93 32 12 3 2 C 3 E - 0 5 8 . 0 C 7 E - C 6 4 nc 2 0 90 2 8 C 4 2 2 8 2 F - 0 5 5 . 7 0 6 E - 0 6 490 31 77 4 9 52 2 6 1 7 E - 3 5 6 . 5 4 2 E - C 6 225 CM IN C L OECL 5 0 0 1 0 . 1 6 6 7 . 3 1 2 . 4 B 4 E - 0 5 6 . 2 U E - C 6 5 1 0 1 0 . 5 4 2 2 . 5 2 3 . 6 6 4 E - C 5 9 . 1 S 9 E - C 6 5 2 0 2 7 . 2 6 6 8 . 1 2 3 . 4 1 9 E - 0 5 B . 5 4 B F - 0 6 3 9 - 5 8 1ST DEMAG SAMPLS 1 2 . 5 - IS C OF CM INCL CECL M J 0 3 5 . 97 1 9 . 0 7 2 . 1 3 3 E - 0 5 5 . 3 3 2 F - 0 6 50 - 4 . 7 9 8 2 . 19 1 . 2 4 9 E - 0 4 3 . 1 2 2 E - C 5 70 3 9 . 6 6 8 5 . 14 3 . 2 7 1 F - 0 5 8 . 1 7 8 F - C 6 90 - 4 9 . 7 1 2 3 . 1 7 7 . 3 9 2 E - C 6 1 . 8 4 PE - C 6 1 80 - 4 5 . 8 0 3 3 . 14 9 . 3 2 1 E—05 2 . 3 3 C E - C 5 250 3 5 . 4 6 7 . 1 2 2 . 4 8 4 E - 0 5 6 • 2 0 9 E - 0 6 2 8 0 31 . 6 6 4 8 . 5 2 1 . 6 7 1 F - 0 5 4 . 1 7 7 F - 0 6 29C 2 3 . 3 1 1 1 . 3 0 1 . 7 4 IE —0 5 4 . 3 5 2 E - 0 6 300 2 5 . 12 3 9 . 7 6 1 . 6 2 3 E - C 5 4 . 0 5 7 E —06 3 5 0 1 9 . 14 1 0 . 0 0 2 . 2 9 2 E - 0 5 5 . 7 2 9 E - 0 6 360 3 5 . 2 3 8 . 1 2 1 . 0 8 6 E - C S 2 . 7 1 5 F - C 6 3 7 0 2 1 . 2 1 2 9 . 0 2 1 . 3 8 5F —0 5 3 . 4 6 3 E —Of 380 3 9 . 0 4 2 3 . 9 4 1 . 5 9 1 E - 0 5 3 . 9 7 8 F - 0 6 43 0 2 9 . 4 0 A * 16 2 . 6 7 9 F - 0 5 6 . 6 9 8 F - C b 4 50 3 0 . 7 8 4 0 . 5 6 2 . 6 9 2 E —0 5 6 . 7 3 1 F - 0 6 4 6 0 - 4 5 . 4 5 7 0 . 8 3 2 . 4 6 1 F —05 6 . 1 5 3 F - 0 6 5 10 1 0 . 7 0 2 9 . 4 4 3 . 3 7 2 F - C 5 8 . 4 3 0 E - 0 6 F 3 9 - 5 8 2ND DEMAG SAMPLS 2 5 - 1 0 0 OF CM IN C L DECL M J 4 . 0 5 7 E - 0 6 4 . 0 4 2 E - C 6 5.270^-06 9 . 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J 5 4 E - C 5 F 2 1 1 2 M NPM M J 0 4 6 F - 0 5 6 . 7 4 3F.-C6 2 6 5 E - 0 5 5 . 4 4 1E-CC 2 7 6 E - 0 5 1 . 5 4 6 E - C 5 2 7 6 E -C 4 ? . 1 2 7 F - 0 6 4 2 3 E - 0 4 2 . 3 7 1 E -C F 2 7 8 E - 9 4 2 . 1 3 1 E - 0 5 4 0 7 E .-0 4 2 • 1 45E -C 5 0U7E —14 1 . 8 1 2E - C r. 5 3 6 E - 0 5 1 . 4 2 3F — 0 5 9 6 C E - 0 5 1 . 1 6 0 F - 0 5 2 9 6 F - 0 4 2 . 1 6 C F - 0 6 9 H 9 E - 0 4 3 . 1 1 4 F -C 5 9 2 1 E -C 5 6 . 5 3 5 F - C 6 4 9 7 E - C 4 4 . 162F.-C 5 3 4 2 F - 0 5 I • 39C E -C 5 6 4 2 E - 0 5 1 . 1 G 7 F -C 5 4 9 7 E - 9 S 1 . 4 1 6 E -C 5 5 5 4 E - 0 4 2 . 5 8 9 E - C 5 3 3 6 E - 0 5 1 . 2 2 3E-C 5 3 9 7 F - 0 5 1 . J 0 5 F - O 5 0 3 R F -C 5 1 ,5 C '■-F-C5 1 2 7 E - 0 5 1 . 3 S 4 F -G 5 9 7 3 F - 0 5 8 . 2 8 9 E - 0 6 62 7 E -0 4 2 . 7 1 2 F - 0 5 7C 1E -C 4 4 • SO 1E — o 5 4 9 7 E - 3 4 4 . 1 6 2 E - 0 5 8 4 0 E - 0 4 3 . O b 6 r —C5 1 0 4 E - 0 4 1 . 0 4 C r - O 5 9 3 6 E - 0 5 3 . 2 2 6 F -C 6 9 0 9 F - 0 5 8 . 1 0 1 5 - C t 2 6 2 E - 0 5 8 . 7 7 1 E - C F 9 4 9 E - 0 5 0 . 2 4 H F - C 6 0 2 7 E - 3 5 6 . 3 7 8 F - 0 6 6 6 7 E - 0 5 7 . 7 7 “ F - C f 1 3 1 E - 0 5 3 • 5 5 2r :-< 6 9 7 C E -C 4 3 . 2 H 3 F - 0 5 2 4 4E-C 4 3 • 7 4 C i — C 5 6 U 6 E - 0 5 7 . 6 7 6 E - C 6 0 0 2 5 " - " 4 1 . 6 7 0 E - 0 5 2 5 1 E- 35 5 . 4 1 9 F - 0 6 9 5 4 F - 4 S 9 . 9 2 3 F - C 6 4 5 9 5 - 0 5 5 . 7 6 6 E -'V - 3 H 4 E -C 4 2 . jc f.e - c * :. 6 5 0 5 - 0 5 7 . 7 ^ 9 8 - 0 6 C 6 4 E - 0 5 1 . 5 1 1 — 0 5 5 4 7 E -C S 1 . 2 5 0 L - C 5 5 8 3 E - C 5 1 . 0 9 7 F - O 5 1 6 5 F -C 4 1 . 9 4 2 F - C 5 6 9 8 E - C 5 6 . 1 6 3 F - C 6 4 8 2 E - 0 5 9 . 1 3 7 E - C 6 4 . i . 5 9 4 • 3 , 9 . 1 . 1 . 1 . 1 . 1 . 8. 6. 1 . 1 . 3 . 2. R. 6. 8. 1. 7 . 6. Q. 0. 4 . I . 2. 2. 1 . 1 . 1 . 4 . 5 . 4 . 3 . 4 . 2. 1 . ? . 4 . 1 . 3 . S . 3 . 1 . 4 . 9 . 7 . 6. 1 • 3 . 5 . 228 CM INCL OECL 6 4 0 - 3 9 06 57 93 6 5 0 35 31 20 75 66C - 2 3 99 7 4 8 5 68C - 4 0 61 74 9 8 6 9 0 - 4 0 15 4 2 98 7 0 0 - 4 4 21 12 9 8 710 30 0 7 8 3 57 7 20 2 85 41 5 9 710 1 7 80 6 5 96 74C - 1 4 33 54 40 750 - 9 25 47 15 760 - 4 95 77 38 7 7 0 - 3 4 1 1 47 24 7 8 0 — 6 26 48 7 6 790 - 1 8 44 71 4 9 8 0 0 - 4 2 70 64 4 6 8 1C — 8 85 82 5 8 8 2 0 - 1 5 85 75 0 9 8 3 0 38 26 80 82 8 4 0 - 3 2 87 56 2 5 8 5 0 - 1 5 10 54 10 8 7 0 - 1 I 4 7 85 6 7 88 0 - 1 4 82 60 4 6 9 0 0 - 1 2 9C 83 33 9 2 0 - 2 2 21 41 94 9 3 0 5 39 70 63 94C — j 5 8 71 4 9 9 5 0 - 3 76 46 28 9 6 0 - 1 3 68 65 96 9 70 - 1 96 78 02 98C - 1 I 62 84 00 9 9 0 - 2 7 83 4 9 71 1 000 - 5 02 6 3 04 M J 7 • 6 2 2 E - 0 5 1 2 7 0 F - C E 1 • 589E —04 2 64 9 E -C S 1 • 2 3 2 E - 0 4 2 3 5 4 1 - — C 5 1 • 2 8 3 E - C 4 2 1 3 8 E - C 5 1 • 6 8 4 E - 0 4 2 8 0 7 E - 0 5 3 • 8 9 3 E - 0 5 6 4 « 9 E - C 6 8 • 7 5 1 E - C 5 1 4 5 8 E - 0 5 7 . 5 5 9 6 - 0 5 1 2 6 0 E - C 5 1 • 2 9 7 E - C 4 2 1 6 2 6 —t 5 1 • 8 5 6 E - 0 4 3 "> 9 3 6 -0 5 1 • 5 5 8 E - C 4 2 59 7 6 - 0 5 9 • 6 7 1 E - 0 5 1 6 1 2 E - 0 5 4 • 4 6 8 E - 0 5 7 4 4 7 F - 0 6 1 • 34 IE —0 4 2 2 3 5 E - C 5 3 • 7 6 3 E - 0 5 6 2 7 1 E - C 6 1 • 3 2 4 E - 0 4 2 2 0 7 6 - 0 5 1 • 4 9 3 E - 0 4 2 4 8 8 E - 0 5 7 . 6 4 2 E - 0 S 1 2 7 4 6 - 0 5 2 . 0 2 3 6 - 0 5 1 3 7 2 E -C 6 1 . 6 1 6 E - 0 4 2 6 9 3 E - C S 1 . 4 4 2 F - C 4 2 4 0 3 E - C 5 1 . 1 5 5 E - 0 4 1 9 2 5 E - C 5 1 . 1 4 2 F - 0 4 1 9 0 4 E - C 5 1 . 1 2 2 E - 0 4 1 3 7 1 E - C 5 1 . 2 1 5 E - C 4 2 0 2 5 E - C 5 8 . 8 9 7 E - 0 5 1 4 8 3 F - C 5 4 • 6 3 1 F - 3 5 7 M 9 f c - ~ 6 1 • 2 7 4 E - C 4 2 1 2 3 E - 0 5 1 • 0 5 9 E - 0 4 1 7 6 6 E - C 5 1 . 2 1 8 F - 1 4 2 0 3 0 E - C 5 1 • 2 4 4 E - 0 4 2 3 7 4 F - 0 5 1 • 6 1 0 E - 0 4 2 6 8 4 E - C 6 1 . 6 7 C E - C 4 2 7 8 4 E —f 5 229 E39-67 1ST DEMAG SAMPLS 150-200 OF CM IN C L DECL M J 40 3 24 25 0 9 7 3 9 8 E - 0 5 1 2 3 3 E - C S 5C - 2 1 82 76 6 7 7 8 6 5 E - C 5 1 31 I E - 0 5 60 4 82 27 6 2 4 9 7 2 E - C 5 8 2 6 7 E - C 6 70 - 9 6 9 69 94 4 9 6 3 5 - 0 5 8 2 72 F — 0 6 I 4C - 1 5 08 6 2 38 5 6 1 6 E - C 5 9 3 6 0 5 — C t 320 2 7 83 3 5 18 4 9 1 9 E - 0 5 8 1 9 9 E - C 6 3 4 0 1 7 40 78 6C 3 3 5 1 E —05 5 5 F 5 F - C F 350 6 25 52 0 7 2 0 7 7 E - O 5 4 T9 4 C - C 6 3 7C - 1 t 21 55 72 6 4 4 2 E - C 5 1 1 7 4 F - C 5 3 0 0 1 57 51 61 6 8 7 7 E - 0 5 1 1 4 6 E - 0 5 390 6 60 6 7 81 7 2 6 7 5 - 0 5 1 21 1 F - C 5 4 3 0 - 1 3 47 62 12 6 1 8 3 5 - 0 5 1 0 3 C F - C S 43 0 21 78 53 6 7 1 3 5 1 5 - 0 5 2 2 6 1 F - C f 4 5 0 9 57 6 8 12 3 7 6 7 E - 0 5 6 2 7 8 E - C 6 4 90 - 4 52 71 4 9 5 3 0 4 E - 0 5 8 8 4 0 6 - 0 6 50 0 1 44 72 3 9 8 3 3 1 E—05 1 J B 9 F - C 5 530 8 52 53 0 7 1 2 6 8 E - 0 5 2 1 1 3 E - 0 6 5 5 0 16 6 5 06 0 9 1 9 6 8 E - C 5 3 2 8 0 E - 0 6 57C 6 8 5 7 54 40 4 9 3 7 C - C 5 8 2 2 8 E - f 6 500 9 06 2 8 5 8 1 5 9 1 E - 0 5 2 6 5 2 E - CC 6 4 0 1 5 1 1 32 70 2 1 6 2 5 - 0 5 3 6 0 3 E - C 6 66C - 6 0 00 29 71 3 3 7 6 E - 9 5 5 6 2 7 E - C 6 7C0 64 21 41 5 9 1 7 4 0 E - 0 4 2 9 0 0 F - 0 5 7 2 0 6 6 6 8 3 20 2 1 6 1 E —05 3 6 0 2 E - C 6 7 4 0 7 89 33 6 5 4 5 6 5 E - 0 5 7 6 G 8 E - C 6 7 5 0 6 91 14 02 1 7 3 6 E - 0 5 2 8 9 3 E - C 6 7 6 0 2 7 9 9 6 4 73 4 4 4 8 E - C 5 7 4 1 4 6 — C 6 7 8 0 1 3 18 69 37 7 3 3 6 E - 0 5 1 2 2 3 6 - 0 5 8 0 0 a 92 44 96 5 3 8 6 E - C 5 8 9 7 6 E - C C 81 0 - 1 2 2 9 70 8 3 5 8 8 5 E - 0 5 Q 3 0 9 6 — C 6 8 2 0 1 5 01 57 4 6 1 6 9 3 E - 0 S 2 8 2 1 6 - C 6 8 4 0 - 1 4 78 6 5 82 8 9 9 9 E - 0 5 1 5 0 0 F - C 5 8 5 0 - 1 4 35 SO 14 3 3 7 0 E - 0 5 5 6 1 7 E - C 6 8 7 0 - 6 67 6 9 37 3 5 9 6 E - 0 5 5 9 9 3 E - C 6 880 - 2 29 5 3 0 7 5 2 2 9 E - 0 5 8 7 1 5 F - C 6 90C - 2 3 14 76 4 2 5 8 4 5 E - 0 5 9 7 4 1 E - 0 6 9 2 0 - 1 0 46 56 25 2 2 9 9 E - 0 5 3 8 3 2 E —06 6 4 0 - 1 2 35 52 0 7 2 92 7 E - 0 5 4 6 7 9 F - C 6 9 5 0 - 1 1 30 53 0 7 4 2 6 3 E - C 5 7 I 0 5 E - 0 6 9 6 0 - 4 72 60 19 5 0 7 2 E - 0 5 8 4 5 4 E - C 6 9 7 0 - 3 ro 85 39 2 3 9 3 E - 0 5 3 9 8 9 E - C 6 IOOC - 2 7 4 5 57 00 5 9 7 9 F - 0 5 9 9 6 5 E - 0 6 F 3 9 - 6 7 2ND DEMAG SAMPLS 1 5 0 —20 0 OF CM IN C L DECL M J 40 1 2 . 4 1 2 4 . 1 2 6 . 8 0 1 E —05 1 . 1 3 4 6 —C 5 72 0 2 . 12 7 4 . 8 5 1 . 6 8 9 E - C 5 2 . 8 1 6 E - O t : 3 9 - 76 3 6 30 S 161 14 F . 37 35 M NKM CM IN C L OECL M J c - 0 92 44 95 3 . 9 0 2 E - 0 4 9 . 7 5 5 E - 0 5 1C - 5 5 42 82 31 5 . 0 2 3 E - 0 4 1 . 2 5 6 E - 0 4 20 - 5 7 f 3 88 78 6 . C C 2 E - 0 4 1 • 5 C C F -C 4 30 - 4 6 94 8 7 82 5 . C 5 9 E - C 4 1 . 2 6 S E - C 4 40 - 6 6 08 81 78 7 . 3 1 2 L - 0 4 1 . 8 2 8 E - C 4 50 - 6 2 H6 63 3b 8 . 2 1 5 E - 9 4 2 . 0 5 4 E - C 4 60 - 6 1 14 74 39 8 . 1 0 8 6 —04 2 . 0 2 76 — 04 70 - 5 5 65 77 82 5 . 3 1 2 F - 0 4 1 . 3 2 8 t — C4 8C - 5 5 78 84 41 5 . 8 3 4 E - 0 4 1 • 4 5 9 F .-C 4 9C - 6 1 10 80 82 6 • 5 8 4 E - C 4 1 • 6 4 6 F - 0 4 IOC - 4 4 92 2 77 5 . 5 0 1 E —04 1 . 3 7 5 6 - 0 4 1 10 - 4 7 6 5 5 1 1 6 . 2 7 C F - C 4 1 . 5 6 8 5 - 0 4 120 - 6 3 25 20 5 3 7 . 9 5 3 E - 0 4 1 . 9 8 8 6 - C 4 1 30 - 4 1 6 5 10 61 9 . 1 1 2 E - C 4 2 . 2 7 8 E - C 4 140 - 3 9 C 5 4 2 1 7 . 2 9 1 E - C 4 1 . 8 2 3E -C 4 1 t o - 4 1 9 6 1? 33 5 . 5 2 8 E - C 4 1 . 3 8 2 E —0 4 1 bO - 6 7 33 18 41 8 . 6 0 2 F - C 4 2 . 1 6 1 F - C 4 1 70 - 4 3 5 6 17 72 7 . 5 7 6 E - 0 4 1 . 8 9 4 F - 0 4 180 - 5 6 05 23 60 6 . 5 4 6 E - C 4 1 • 6 3 7 L - C 4 19C - 5 8 28 3 57 6 . 3 8 4 E - C 4 1 . 5 9 6 E - C 4 2 00 - 4 4 81 5 70 2 . 9 6 J E - 0 4 7 • 4 0 HE — Of 21 0 - 4 3 C 2 6 70 1 . 4 6 9 E - 0 4 3 • 6 7 3 E - 0 6 22 0 - 4 0 9 26 54 1 . 1 7 1 E - 0 4 2 . 9 2 8 6 - 0 6 2 30 - 5 3 60 12 25 8 . 3 C 2 E - 0 5 2 . 0 7 6 6 - 0 5 2 4 0 - 1 9 78 16 2 4 5 . 5 5 3 E - 0 5 1 • 3 8 8 6 —C 5 2 50 - 4 7 53 43 1C 6 . 7 9 5 E - 0 5 1 . 6 9 9 E - C 6 2 6 0 - 3 2 52 43 10 6 .4 3 8 1 - 0 5 1 . 3 6 0 E - 0 5 27C - 4 4 C 8 22 81 6 . 0 0 3 E - 0 5 1 . 5 0 IF . - t 5 2RC - 6 7 37 46 50 4 . 2 7 7 E - 0 4 1 . 9 6 9 6 - 0 4 2 9 0 - 6 7 02 58 9 7 4 . 6 9 7 E - 0 4 1 . 1 7 4 C -C 4 30C - 6 2 6 2 18 4 1 6 . 9 1 5 E - 0 4 1 . 7 2 9 E - 0 4 31 0 - 5 3 5 2 19 16 8 . 5 7 2 E —0 4 2 .1 4 3 E - 0 4 320 - 6 6 74 18 41 7 . 2 4 3 E —04 1 . 8 1 1 E —C 4 33C - 6 7 31 30 9 3 5 . 7 0 5 E - 0 4 1 . 4 2 6 E - C 4 340 - 6 1 C 7 20 53 7 . 3 9 8 F - 0 4 1 . 8 5 0 6 - 0 4 3 50 - 6 5 89 42 2 1 5 . 5 4 9 8 - 0 4 1 , 3 8 7 t - C 4 360 — 67 PC 2 6 64 4 .9 6 3 1 — C 4 1 • 2 4 1!; — C 4 3 7 0 — 62 6 9 29 02 9 .4 0 .3 E — 04 2 . 3 5 1 F -0 4 380 - 5 8 72 36 83 8 . G 6 5 E - C 4 2 . 9 1 6 6 - 0 4 3 9C - 1 7 72 3 6 C 6 3 . 9 1 I E - 0 4 9 . 7 7 6 E - 0 5 4 0 0 - 6 9 23 11 30 6 . 0 3 2 E - C 4 1 . 5 0 BE —04 4 1 C - 6 5 44 3 81 2 , 2 7 4 E —04 5 . 6 8 4 6 - 0 5 420 - 7 5 05 7 69 3 . 6 9 8 E - 0 4 9 . 2 4 4 E - C 5 4.3C - 7 1 29 15 62 5 . 0 9 5 E - 0 4 1 . 2 7 4 '* —C4 44 0 <*9 18 5 0 6 7 . 6 1 6 E - 0 4 1 . 9 C 4 F - C 4 45C 60 0 2 10 OC 4 . 3 4 C F - 0 4 1 . 9 8 5E — C 4 4 6 0 6 5 26 6 20 5 . 5 2 5 E - 0 4 1 . ' 8 1 E—04 4 7 0 50 28 6 0 7 4 . 6 4 3 E - C 4 1 . 1 6 1 E - 0 4 480 - 6 1 5 8 1 3 38 9 . 5 0 0 E - C 4 2 . 3 7 5 6 - 0 4 49 0 - 6 4 77 15 9 3 6 . 4 4 2 E - C 4 1 .6 1 1 r —C 4 CM 530 5 I C 52C 5 3 0 54C 5 5 0 5 6 0 5 7 0 5 8 0 59C 60 C 61 0 6 2 0 6 3 0 6 4 0 6 5 0 6 6 0 6 70 6 0 0 690 70 0 71 C 7 2 0 73 0 7 4 0 7 5 0 7 6 0 7 7 0 7 8 0 7 9 0 8 0 0 8 1 0 82 0 8 3 0 8 4 0 8 5 0 8 6 0 8 7 0 8 8 0 8 9 0 90C 9 1 0 9 2 0 9 3 0 9 4 0 9 5 0 96C 9 7 0 9 8 0 9 9 0 231 I NCL I'fTCL M J - 6 0 f 3 17 51 r> 1 05F - ? 4 1 ? 7 6E -C 4 - 5 9 89 18 41 5 9 4 G F - C4 1 4 8 F P - C 4 - 5 0 2 5 27 65 6 7 6 3F.-0 4 I 6 9 1 F - C 4 - 5 4 53 2b 2 5 4 3 0 8 5 - 0 4 1 0 7 7 F -0 4 - 3 9 04 23 94 1 5 9 1 5 - 0 4 3 9 7 8 F - C 5 - 5 1 59 3 81 1 5 1 9 E - 0 4 3 7 9 8 E -C 5 - 5 3 ?4 6 3 36 2 3 4 6 F - C 6 5 B 6 5 F - 0 7 - 2 9 17 26 54 6 4 2 5 F - 0 6 1 6 C 6 F - C 6 - 4 8 52 36 83 1 4 2 2 E - C 5 3 5 5 4 F - C 6 - 4 5 81 74 9 8 4 6 5 9 F - 0 5 1 16 5 F - C 5 - 6 6 50 86 33 1 6H61 — C 4 4 2 1 4 E -C 5 - 7 b 67 2 5 1 7 1 5 9 6 L - C 4 3 9 8 9 E - C 5 - 7 4 39 36 83 3 9 0 4 F - 0 5 9 7 6 1E —C 6 - 6 1 12 71 4 9 1 6 4 6 E - 0 5 4 1 1 4 E - C 6 - 2 9 56 77 71 5 4 S 9 E - 0 5 1 3 6 5 E - C 5 - 8 4 85 44 95 1 0 C 7 E - 0 4 2 5 1 8 E - 0 5 - 6 3 25 20 5 3 3 9 7 6 E - 0 5 9 94 1 F -C 6 - 7 4 35 2 8 27 3 4 5 0 E -C 5 8 6 2 4 F - C 6 - 5 0 19 46 9 2 2 0 1 2 F - 0 4 5 9 2 « E - 0 5 - 4 3 64 6 5 7 1 51 3 E -C 4 3 7M 2F-C 5 - 5 4 57 27 3 2 1 1 7 9 E -C 4 2 94 7 E - 0 5 - 6 4 70 5 7 32 1 4 5 6 F — 04 3 6 3 9 F - 0 5 - 5 4 01 32 28 2 C 6 5 E - 0 4 5 1 6 2 F - 0 5 - 1 5 17 2 6 6 7 1 C 3 7 E - C 4 2 5 9 3 F - C 5 - 6 6 6 8 14 02 1 0 9 2 F - 0 4 2 73CF.-0 5 - 4 0 56 4 5 7 1 3 8 1 E - C 4 3 4 5 2 T - C 5 - 3 9 30 2 6 54 3 6 2 6 F - 0 5 9 •J65L-C 6 - 6 5 48 5 3 0 7 2 5 2 5 E - 0 5 6 3 1 3 E - 0 6 - 7 1 51 75 8 8 3 0 5 0 E - 0 5 7 6 2 6 F - 0 6 - 5 8 78 77 38 1 4 9 0 E - C 4 3 7 2 4 E - C 5 - 6 8 16 79 61 6 3 0 1 E—05 1 5 7 5 F - C 5 - 6 5 6 ? 34 6 6 8 0 2 7 E - 0 5 2 0 0 7 E - C 5 - 5 1 97 23 72 9 2 7 9 E - 3 5 2 3 2 0 5 - 0 5 - 5 3 09 62 0 3 2 01 I F - 0 4 5 02 8F.-C5 - 5 8 96 58 5 6 1 9 5 0 E - C 4 4 R 7 5 E -C 5 - 7 4 0 3 82 78 1 8 4 7 E - 0 4 4 6 1 8 E - 0 5 - 6 5 21 8 6 5 4 2 5 5 4 E - 0 4 6 3 8 5 E - C 5 - 2 8 0 8 30 70 1 0 2 0 F - 0 4 2 5 5 0 F - 0 5 - 7 4 16 74 27 1 9 9 8 E - 0 4 4 9 9 5 E - C 5 - 5 8 50 78 91 1 4 7 0 E - 0 4 3 6 7 4 F - C 5 - 4 9 68 80 32 2 3 2 8 E - 0 4 5 8 2 1 E - 0 5 - 4 7 37 61 8 6 3 1 5 1 E - 0 4 7 8 7 7 F - C 5 - 1 6 25 6 8 12 2 4 6 2 E - 0 4 6 I 5 5E - 0 5 - 6 1 17 77 38 6 0 0 8 E - 0 4 1 5 C 2 E - 0 4 - 6 2 91 78 60 2 8 1 5 E - 0 4 7 0 3 8 E - 0 5 - 8 4 60 68 I 2 1 2 1 7 E - C 3 3 0 4 4 F —04 - 8 7 44 63 36 1 0 8 8 E - 0 3 2 7 2 0 F - 0 4 - 0 74 8 9 6 1 6 0 8 E - C 3 4 0 2 1 E - C 4 - 1 87 1 8 8 1 2 7 6 F - 0 3 3 1 9 1 F - C 4 - 3 7 25 44 95 4 8 3 0 E - C 4 1 20 7 F - 0 4 r 3 9 - 7 6 1ST n> MAG SAMPLS IC C -4 0 C n - CM IN C L n t C L 0 - 3 . 1 4 5 0 . 14 J . 4 3 3 t —04 8 S B 3 F -C 5 1 c - 6 5 . 5 4 7 8 . 6 0 3 . 0 9 B E - 0 4 7 74 4fc- 0 6 100 - 4 3 . 4 0 3 8 . 3 2 2 . 6 4 4 T - 04 6 6 1 C L -C S 2 0 0 - 4 4 . 2 1 1 2 . >8 2 . 3 3 OF - 0 4 6 84 CF- C* 2 1C 4 1 .4 1 6 . 3 .3 7 . 5 7 6 5 - 0 5 1 8 9 4 F - C 6 2 2 0 - 2 . 0 2 44 . 9 5 1 . 1 83F - 0 4 2 '>68>' - 0 6 2 3 0 - 5 3 . 7 8 H . 74 4 . 6 5 9 E - C 5 1 I 65L - 05 2 4 0 -1 . 5 4 3 6 . 2 1 7 . 7 7 8 F —0 5 1 9 4 6 r - r> 5 2 SC - 5 4 . 8 4 1 8 .4 1 2 . 2 9 9 L —0 5 5 74 7L-0C. 26C - 6 8 . 15 51 . 2 8 7 . 6 2 2 5 - 0 5 1 9 0 6 E - 0 5 4 1 C - 7 1 . 0 7 4 9 . 3 4 5 . 9 6 3 E - 0 5 1 4 9 1 F - 0 5 4 3C - 6 5 . 1 7 1 8 . 4 1 1 . 1 C 5 E - 0 4 2 7 6 2 E - 1F 4 ec -60.5 1 4 . 2 1 3 . 4 5 5 r — r 4 8 9.3 8 F - 0 6 56C - 2 4 . 1 1 6 0 . 14 1 . " 7 3 E - C 5 2 6 8 3F.-C6 5 9 0 - 2 9 . C4 7 6 . 5 2 1 .5 4 9 E - 0 5 7 8 71 F - 0 6 6 2 0 - 5 7 . 8 8 7 9 . 2 9 1 . 9 2 3 E - 0 5 4 6 C R F -0 6 6 7 0 - 2 3 . 1 8 6 8 . 9 7 1• 591 E - 0 5 3 9 78fc -C 6 6 HO - 5 0 . 1 8 3 4 . 2 5 8 . 7 0 1 E — 0 5 2 1 7 5 F -C 5 69C - 6 4 . 8 5 60 . 8 8 5 . C 7 7 F - C 5 1 2r»9r - 0 5 7 7C - 1 0 . 4 3 4 2 . 4 6 6 • 9 1 9 t - 3 5 1 7 1 0 E -C 5 7 7 C - 6 5 . 6 7 3 3 . 6 5 1 . 8 .34- - 6 5 4 >85F-Cf. 7 HO - 6 0 . Cf 8 2 . 2 1 1 . 66 7F.-0 4 3 9 1 7f - 1 5 790 - 1 8 . 9 6 4 4 . 9 6 1 . 1 5 7 E - 9 4 2 89 1 F -C 5 >10 - 3 1 . 3 4 2 6 . 5 4 6 . 0 2 1 E - C 5 ! 5 C 5 E - 0 5 9 2 0 - 1 6 . 4 9 7 4 . 0 8 S . 0 7 6 F —05 1 _ r 6 9 3 0 - 7 9 . 4C 4 4 . 9 5 1 . 2 9 7 E - C 4 3 2 4 2 E - C 5 9 4 0 - 6 6 . 7 4 1 5 . 9 3 3 . 8 6 5 E - C 5 9 6 6 fy -Cf 9 7 0 4 6 . 52 2 7 . 7 9 1 . 2 3 8 C - C 4 3 0 0 < tF -f 5 9 8 0 5 8 . C 1 3 5 . 32 1 . S 0 2 F - 0 4 3 7 6 6E - C * 9 9 0 3 . 4 1 7 9 . 6 1 7 . 0 2 3 F - 0 5 I 756F- 0 5 V I - 7 6 2ND Of MAG SAMPLS 2 O C -R 0 0 CIE CM INCL CECL 0 - 1 . 34 50.66 1C -51.31 67.64 20 C -41.66 19.63 2 2 C 8. 24 29.E 1 2 30 -51.11 11.30 240 41. c e 75.38 2 60 — 3C• 1 3 54 .40 M J 2.674E-04 6 . 66*006 6 • 1 5 4 E - 0 5 1 . 5 7 3 E - C 6 1 . 6 6 5 F - 0 4 4 .1 6 2 F . - C 6 7.282E-05 l.«2ir-<-‘ - 5 .C 9 8 F . - 0 5 1 . 7 7 S E - 0 5 1 . 7 1 6 F - 0 5 4.29CE-Ct 2 . 0 8 C F - 0 5 5 .1 9 9 F . - C * C 3 9 - 7 6 3RD Of MAG S A M > ■ * I S 2 5 0 -4 C O OF CM INCL OECL M r - 1 . 4 1 5 0 . 7 5 1 . 7 5 6 0 0 4 4 .3 Q C F .-C S 2 0 0 - 3 3 . 1 9 3 . 5 7 8 . C 1 C F - C 5 2 . C 0 3 F - ‘ 5 f J O - 4 3 . 9 7 1 4 .9 1 4 . 5 1 2 E - 0 5 1 . 1 2 3 F - C 6 IS O - 3 9 . 72 3 3 . 6 5 9 . 8 C 3 p - 0 6 ? . 4 6 1 0 0 233 F 3 9 - 7 6 4TH DtMAG SAMPLS 4 0 C -6 C O 9E CM INCL D iC L M J 0 1 8 . 5 5 2 9 . 5 7 3 . 3 4 7 F - 0 5 0 . 3 6 B F - O 6 23C - 2 8 . 6 5 4 3 . 1 0 5 . 2 2 5 E - C 5 1 . 3 C 6 F - P 5 23C 4 9 . 5 9 1 1 . 3 0 3 . 2 9 1 C - P 5 8 . 2 2 8 E - 0 6 E 3 9 - 76 TRIGGER CORF NRM CM IN C L OECL M J 5 - 5 7 . 1 9 3 9 . 7 6 6 . 3 3 7 F - 0 4 1 . 5 8 4 E - C 4 35 - 3 2 . 0 9 2 3 . 6 8 6 . 6 9 0 E - 0 4 1 . 6 7 2 E - C 4 5 5 - 3 9 . 9 3 0 5 . 6 9 7 .0 O O E -O 4 1 . 9 5 C r - 0 4 E 3 9 - 7 6 TRIGGER COHF 2 0 0 OF CM IN C L DECL M J 5 - 5 4 . 8 1 3 3 . 6 5 3 . 1 4 3 F - 0 4 7 . 8 5 8 F - C 6 » APPENDIX II FORTRAN IV program used to reduce and plot the paleomagnetic data. 234 'OOOOG OO O 0 0 0 0 0 0 0 0 9 0 o o o o o o o o o o o o o o o o o o o o o o o o o o o o n O O O O O O O O 0 0 0 9 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 o o o o o o o o o o o o o o o u o o o o UUUUUUUUUUMMNMUMMNIV) fOHXMMMKHMi-HOOOOOOOOO s( mji>u n >*o oa>Noyt»ufv)'-ooci)^o>ui*'ur\)—o>oa>jo^4>ojoj-ooai>(oj>frurv)- SO o n o o o o *•-»<> a ^ —-> a r ro u t* IMA AM M A — fjl ci r ~ II ~ z n z ^ n A • Z to* ***•• m • o » - - u c o s - > > n Z H Z — |/1 — . t y . jj> *«0 7 uicn n x T lO D X O l I - t i\* IV J • • « I I U I H H -4 • T l f\)» • m m m H M z r r x « ^ U 1 • o»*** ro yi w i U W W \'I|O N \» h i- *- r\>ui» 0 0 * •* J 3 O II *• H « • w •d —• » o o W fu «*«* > <0 U I • • w • n o o - o o > w*-*- > s * *- > a \ — • « — # ro to** • Z w • w 0 ^ *** • • r> • ^ T s > > • • M H « w ^ • Id < • «I7 ^ roc 0 • > J •- N C l -4 * > * * O •0 0*+ O * m - 4 0 • 0 to 0 X * N O ► > h h n > h » « • — r 0 cn>no' 0 to** • *0 X Id Z z • • — * » toto 0 ► ate -4 • ~ 0 • • to -0 *0 O ' ~i a * « « z • A h h JJO A to cn* X O N N OO • « ♦ ♦ 0 rn a t o • a t_ • < ■ < • • P X w • • * M w • | • to ** — a w OO — I > > • 3i 2 •* U O *n *-» a 0 MM > W • II w H 03 • > ♦ • •0 > • to +0 rj 0 0 4 « > • • ** *o~ • • • • « — A ¥0 • • m O N N - w X rn • 0K A w • • W •0 0* •- 0 1 N > > ♦ t\) •M z to w * II H 0 • • M M > • » - * • 0 U > • • — m • I w w toto — 0 7 n • 00 + 0 w • • w ■ < • ( /> u 0 A n • • « v • to z * r r * 0 0 • -4-4 * W 0 X • • IV) « * C \ 0 0 • 0 0 0 0 0 • • □ z or* n ■ H r V w O • 0 0 0 0 n n Q n z H r -to • a ■ 5 O ' • <JiO « _ - r I Z r > r o m n S£3 o o o o o o o o o o o o o o o o o o o o o o ra o o o o o o o o o OOOOOOOOOOQOOOOOOOOOOOOOo o o o o o o o SHHHHHHHHH(MM)<0>(M>0><Mn9i010l010l W01010IWIJI** «®HO'UI*UM**OioaH<MJI*UIV)**0<0®HO' 0 1 »W IV)** oo® r o O’ u i mi/>oo z H>» oorr nrr mu zr ■ O H rr HZ — X <T> X • • O H • H U« • X • O x *- I f ) O HX H ><x h r h m z r hoc H • * Z ♦© I I C* H Z< H DO Z r c * ♦ OHHO OHH* z i i r ioc i r OIZUI I I • U z i nr I I t o h *-h r • o z r u • « o X 0 > o o h at H H — O a < j i • H H Z C z 0 <x * <x r ii z roc • 2 zoii c z Z I ■ o * * r X O ZX oo «O H n>> i i * - i i i r r x*-o i rr • c n ii • — ♦ >• DD -zxorr • i i r ho o- * ♦ r h z * H O H H - I • O c 0 1 ■ H • O a 0 1 x X Z C £ Z ~ *»o I • oo • • — i • r o ro* • U l U l * • ui f r * - X 000 >>> rrr r rr n>v t x r >»-o V < / > H A ^ A ^ OO • • • iO oo • • • 1 I i OfUfV) • • • a wu • • • a**u • * * — oi r • ~ • OZ I? 0 1 r o < « i I V ) * * 01® oo oz»on > H x n » r-rzr r o i i nr I I x« >>~z< x x*cn «r xrno o> * — H — •► * o < _ » • u . o — I IV) • U J « I V ) x ro > x r X O T f T I • OO O inn • t i » - ■ H * • X -* o Z • o w p ~ • • ® U l X X O O i-i o > T r n r * o — < * • NKIi OIOO OHO O* 7 ) 1 0 X • o HC • AH X3 * a oo r - z » X ro in - 0 0 0 1

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University of Southern California Dissertations and Theses

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Creator Theyer, Fritz (author)

Core Title Late-Neogene Paleomagnetic And Planktonic Zonation, Southeast Indian Ocean - Tasman Basin

Degree Doctor of Philosophy

Degree Program Geological Sciences

Publisher University of Southern California (original), University of Southern California. Libraries (digital)

Tag Geology,OAI-PMH Harvest

Language English

Contributor Digitized by ProQuest (provenance)

Advisor Bandy, Orville L. (committee chair), Gorsline, Donn S. (committee member), Pieper, Richard E. (committee member)

Permanent Link (DOI) https://doi.org/10.25549/usctheses-c18-771882

Unique identifier UC11364226

Identifier 7300779.pdf (filename),usctheses-c18-771882 (legacy record id)

Legacy Identifier 7300779

Dmrecord 771882

Document Type Dissertation

Rights Theyer, Fritz

Type texts

Source University of Southern California (contributing entity), University of Southern California Dissertations and Theses (collection)

Access Conditions The author retains rights to his/her dissertation, thesis or other graduate work according to U.S. copyright law. Electronic access is being provided by the USC Libraries in agreement with the au...

Repository Name University of Southern California Digital Library

Repository Location USC Digital Library, University of Southern California, University Park Campus, Los Angeles, California 90089, USA