1962 1962-01 Scotese, C.R., 1962. “Snuffy” Big Shoes Summer Vacation Journal (unpublished), 48 pp. ResearchGate Academia 1963 - 1967 1967-01 Scotese, C.R., 1967. A Review of Paleontology by Eras and Periods, Volume 1. Precambrian to Silurian, Chicago, IL. ResearchGate Academia 1974 1974-01 Scotese, C.R., 1974. The first vertebrate flying machine, Earth Science, 27:145-150. (1b) ResearchGate Academia 1974-02 Scotese, C.R., 1974. The evolution and biogeography of lower Paleozoic crinoids in relation to the tectonic history of the proto-Atlantic, Geological Society of America, North-Central Section, 8th Annual Meeting, 6:543-544. ResearchGate Academia 1974-03 Scotese, C.R. 1974. First Flip Book Images (from 35mm film from PLATO System), Unpublished. (1a) ResearchGate Academia 1974-04 Scotese, C.R., 1974. The evolution and biogeography of Lower Paleozoic crinoids in relation to the tectonic history of the Proto-Atlantic, Walker Museum Memorial Lectures, Deoartment of Geology, University of Chicago, May 16, 1974. ResearchGate Academia 1975 1975-01 Scotese, C.R., and Baker, D.W., 1975. Continental drift reconstructions and animation, Journal of Geological Education, 23: 167-171. (2) ResearchGate Academia 1975-02 Scotese, C.R., 1975. Continental Drift Flip Book, 1st edition. Chicago, Illinois. (single page version) (3a) ResearchGate Academia 1975-03 Scotese, C.R., 1975. Continental Drift Flip Book, 1st edition. Chicago, Illinois. (double page version) (3b) ResearchGate Academia 1975-04 Scotese, C.R., 1975. Computer Drawn Continental Drift Reconstructions, Department of Geological Sciences, University of Illinois, Chicago, Chicago, Illinois 60680. (2b?) lost scan, redo ResearchGate Academia 1975-05 Ziegler, A.M., 1975. A Proposal to Produce an Atlas of Paleogeographic Maps, Department of Geophysical Sciences, University of Chicago, June 1975. (3c) ResearchGate Academia 1975-06 Ziegler et al., 1975. Standard Procedures for Paleogeographic Data Compilation and Interpretation, Assembled by A.M. Ziegler for the compilers, consultants, and reviewers of the forthcoming ATLAS OF PALEOGEOGRAPHIC MAPS, First Edition, November 1975, Department of Geophysical Sciences, University of Chicago, 50 pp. lost scan redo “blue book” ResearchGate Academia 1975-07 Vail presentation & photo of participants ResearchGate Academia 1976 Milestones: Start Graduate School at U. Chicago 1976-01 Scotese, C.R., 1976. Continental Drift “Flip Book”, edition 1.5, Department of Geological Sciences, University of Illinois. ResearchGate Academia 1976-02 Scotese, C.R., 1976. A continental drift “flip book", Computers & Geosciences, 2:113-116. (4) ResearchGate Academia 1976-03 Scotese, C.R., and L.W. Ethetton, 1976. A computer drawn animation of continental drift, First Annual Student Conference in Earth Sciences, abstract with program, University of Wisconsin, Milwaukee. ResearchGate Academia 1976-04 Ziegler, AM., Hansen, K.S., Johnson, M.E., Kelly, M.A., Scotese, C.R., and R. Van der Voo, 1976. Silurian continental distributions, paleogeography, climatology and biogeography, International Geological Congress, Symposium 103.5, Past Distribution of Continents, Abstracts, Issue 25, v. 3, p. 729. ResearchGate Academia 1977 1977-01 Ziegler, A.M., Scotese, C.R., McKerrow, W.S., Johnson, M.E., and Bambach, R.K., 1977. In Paleontology and Plate Tectonics with Speacial Refernce to the Tectonic History of the Atlantic Ocean, R. M. West, ed., Paleozoic biogeography of the continents bordering the Iapetus (pre-Caledonian) and Rheic (pre-Hercynian) ocean, Milwaukee Public Museum, Contributions in Biology and Geology, 2:1-22. (5) ResearchGate Academia 1977-02 Ziegler, A.M., Scotese, C.R., and Bambach, R.K., 1977. Paleozoic biogeography of continents bordering the Iapteus (pre-Caledonian) and Rheic (pre-Hercynian) oceans, North American Paleontological Convention II, Journal of Paleontology, volume 51, Issue 2, Suppl., Part III, p. 33. ResearchGate Academia 1977-03 Ziegler, A.M., Hansen, K.S., Johnson, M.E., Kelly, M.A.,Scotese, C.R., and Van der Voo, R., 1977. Silurian continental distributions, paleogeography, climatology, and biogeography. Tectonophysics, 40: 13-51. (6a) ResearchGate Academia Abstract: Continental orientations during the Silurian period have been determined using paleoclimatic in addition to paleomagnetic data. Good morphological fits are obtained for India and Australia to Antarctica in the Mesozoic. In the late Paleozoic east and west Antarctica seem to be separated by large tracts of oceanic crust and there may have been movement between the two. Gondwana, incorporating East Antarctica and possibly West Antarctica, was by far the largest land area in Silurian times. All of the paleocontinents were in relatively low latitudes with the exception of Gondwana which was over the South Pole. In the early Silurian subtropical highs of the southern hemisphere probably expanded over the continental land masses, where anticyclonic patterns were thermally reinforced by winter cooling of the land. This would have occurred above the Australian-Antarctic portion of Gondwanaland, where a north-south oriented pressure ridge would merge the subtropical high pressure into a cold, massive cell located at higher latitudes above the continental interior. During the summer, monsoon-like rains would have occurred in Antarctic Gondwanaland. Polar regions of Gondwanaland are expected to have been extremely dry due to isolation from moisture supplies. Intense cold would have prevented the melting of snow, creating a potential for glaciation as in the present-day Antarctica. 1977-04 Ziegler, A.M., 1977. Common Paleogeographic Fallacies, Department of Geophysical Sciences, University of Chicago. (11c) ResearchGate Academia 1977-05 Ziegler, A.M., and Scotese, C.R., 1977. Thoughts on Format for the Forthcoming, “Atlas of Paleogeographic Maps”, Department of Geophysical Sciences, University of Chicago. (6b) ResearchGate Academia 1978 1978-01 Scotese, C.R., and Ziegler, A.M., 1978. Paleozoic continental drift reconstructions and animation, American Geophysical Union, 1978 Spring Annual Meeting, Eos, v. 59. Issue 4, p. 263. ResearchGate Academia 1978-02 Ziegler, A.M., and Scotese, C.R., 1978. Thoughts on Format for the Forthcoming “Atlas of Paleogeographic Maps”, Department of Geophysical Sciences, University of Chicago, Chicago, IL. ResearchGate Academia 1979 1979-01 Ziegler, A.M., Scotese, C.R., McKerrow, W.S., Johnson, M.E., and Bambach, R.K., Paleozoic paleogeography, Annual Review of Earth and Planet Sci., v. 7, p. 473-302. (9) ResearchGate Academia 1979-02 Scotese, C.R., Bambach, R.K., Barton, C., Van der Voo, R., and Ziegler, A.M., 1979. Paleozoic base maps, Journal of Geology, 87:217-277. (7a) ResearchGate Academia 1979-03 Bambach, R.K. and Scotese, C.R., 1979. Paleogeographic reconstructions: the state of the art, Short Course notes, SE section, Geol. Soc. Amer., Blacksburg, VA, 111 p. (7b) ResearchGate Academia 1979-04 Scotese, C.R., 1979. Phanerozoic Continental Drift Base Maps, in Paleogeographic Reconstructions: State of the Art, by R.K. Bambach and C.R. Scotese, SE section, Geol. Soc. Amer., Blacksburg, VA, 30 p. ResearchGate Academia 1979-04 Scotese, C.R., 1979. Continental Drift (flip book), 2nd edition. (8) lost scan redo ResearchGate Academia 1979-05 Scotese, C.R., 1979. Plate Tectonic Regulation of Global Species Diversity, Research Paper, Department of Geophysical Sciences, University of Chicago, 48 pp.44 ResearchGate Academia 1980 1980-01 Scotese, C.R., Snelson, S.S., and Ross, W.C., 1980. A computer animation of continental drift, J. Geomag. Geoelectr., 32: suppl. III, 61-70. (11b) ResearchGate Academia 1980-02 Scotese, C.R., 1980. Mesozoic and Cenozoic paleocontinental maps, by Smith, A.J., Briden, J.C., (book review), American Journal of Science, v. 280, p. 93-96. (11a) ResearchGate Academia 1980-03 Bambach, R.K., Scotese, C.R., and Ziegler, A.M., Before Pangaea: The paleogeographies of the Paleozoic world, American Scientist, 68:26-38. (10) rescan in color ResearchGate Academia 1980-04 Van der Voo, R., and Scotese, C.R., 1980. Great Glen Fault: 2000 km of sinistral displacement during the Carboniferous, American Geophysical Union, 1980 Spring Annual Meeting, Eos, v. 61, Issue 17, p. 220. ResearchGate Academia 1980-05 Scotese, C.R., 1980. Paleomagnetic results from the siderite nodules of Mazon Creek, Illinois, American Geophysical Union, 1980 Spring Annual Meeting, Eos, v. 61, Issue 48, p. 1196. ResearchGate Academia 1981 1981-01 Ziegler, A. M., Barrett, S. F., and Scotese, C.R., 1981. Paleoclimate, sedimentation and continental accretion, in the Origin and Evolution of the Earth's Continental Crust, S. Moorbath and B.F. Windley, eds., Philosophical Transactions of the Royal Society of London, Series A: Mathematical and Physical Sciences, A301:253-264. (13) 1981-02 Scotese, C.R. and Van der Voo, 1981. Carboniferous directions from Early Devonian limestones (Helderberg Group) of New York, American Geophysical Union, 1981 Spring Annual Meeting, Eos, v. 62, Issue 17, p. 274. 1981-03 Ziegler, A. M., Parrish, J. T., and Scotese, C.R., 1981. Cambrian world paleogeography, biogeography and climatology, M.E. Taylor (editor), Short Papers for the Second International Symposium on the Cambrian System. Open File Report, U.S. Geological Survey., OF 81-0743, p. 252 (14a) 1981-04 Scotese, C.R., Snelson, S., Ross, W.C., Dodge, L.P., McElhinny, M.W., Khramov, A.N., Ozima, M., and Valencio, D.A., 1981. A computer animation of continental drift, Advances in Earth and Planetary Sciences (AEPS),v. 10, pp. 61-70. 1981-05 Van der Voo, R., and Scotese, C.R., 1981. Paleomagnetic evidence for a large (2,000 km) sinistral offset along the Great Glen fault during Carboniferous time, Geology, 9: 583-589. (12) 1981-06 Scotese, C.R., Van der Voo, R., and Ross, W.C., 1981. Mesozoic and Cenozoic base maps, 1981 AAPG Annual Convention, v. 65, Issue 5, p. 989. 1981-08 Ziegler, A. M., 1981. Paleozoic Paleogeography, in Reconstruction of the Continents, Geodynamics Series, volume 2, American Geophysical Union, p.31-37. 1981-09 Ziegler, A.M., Bambach, R.K., Parrish, J.T., Barrett, S.F., Gierlowski, E.H., Parker, W.C., Raymond, A.L., and Sepkoski, J.J., Jr., 1981. Paleozoic biogeography and climatology, Chapter 7, in K.J. Niklas (editor), Paleobotany, Paleoecology, and Evolution, Volume 2, Praeger Publishers, New York, p. 231-266. 1982 1982-01 Van der Voo, R., and Scotese, C.R., 1982. Comments and Reply on “Paleomagnetic evidence for a large (~2000 km) sinistral offset along the Great Glen Fault during Carboniferous time”, discussions and reply, Geology v. 10, p. 487. (17) 1982-02 Scotese, C.R., Van der Voo, R., and McCabe, C.,1982. Paleomagnetism of the Upper Silurian and Lower Devonian carbonates of New York State: Evidence for secondary magnetizations residing in magnetite, Physics of the Earth and Planetary Interiors 30:385-395. (16) 1982-03 Parrish, J. T., Ziegler, A.M., and Scotese, C.R., 1982. Rainfall patterns and the distribution of coals and evaporites in the Mesozoic and Cenozoic, Palaeogeography, Palaeoclimatology, Palaeoecology, 40: 67-101. (19a) 1982-04 Ziegler, A.M., 1982. Paleogeographic atlas project, background, current status, future plans, University of Chicago. (19e) 1982-05 Peinado, J., Van der Voo, R., and Scotese, C.R., 1982. A reevaluation of Pangea reconstructions, American Geophysical Union, 1982 Spring Annual Meeting, Eos, v. 63, Issue 18, p. 307. 1982-06 Van der Voo, R., Scotese, C.R., and McCabe, C., 1982. Was there an Eocambrian supercontinent before the Paleozoic Wilson Cycle?, American Geophysical Union, 1982 Spring Annual Meeting, Eos, v. 63, Issue 18, p. 308. 1982-07 Scotese, C.R., and Van der Voo, R., 1982. Carboniferous paleomagnetic results from Nova Scotia and Cape Breton, American Geophysical Union, 1982 Spring Annual Meeting, Eos, v. 63, Issue 18, p. 307. 1982-08 McCabe, C., Peacor, D.R., Scotese, C.R., Van der Voo, R., and Friedman, R., 1982. Magnetizations residing in diagenetic magnetite in the Devonian Helderberg Group Limestones, American Geophysical Union, 1982 Spring Annual Meeting, Eos, v. 63, Issue 18, p. 305. 1982-09 Scotese, C.R. and Van der Voo, R., Paleomagnetism, plate tectonics, and paleogeography: course report #1, Geol. Sci. 607, Tectonics Seminar, Winter 1982, Ann Arbor, Michigan. (19d) 1982-10 Van der Voo, R., and Scotese, C.R., 1982. Comments and Reply on “Paleomagnetic evidence for a large (~2000 km) sinistral offset along the Great Glen Fault during Carboniferous time”, discussions and reply, Geology v. 10, p. XXX. (18) 1982-11 Friedman, R.M., and Scotese, C.R., 1982. A summary of Paleomagnetic data for the Cordillera of western North America, University of Chicago. (19c) 1982-12 Overbye, D., 1982. The Shape of Tomorrow: An imaginative Chicago geologist plots the wanderings of the continents to try to read the shape of the future, Discover, volume 3, number 11, p. 20-25. (19b) rescan in color 1982-13 Parrish, J.T., 1982. Upwelling and Petroleum Source Beds, with Reference to the Paleozoic, American Association of Petroleum Geologists Bulletin, v. 66, no. 6 (June), p. 750-774. (19g) 1982-14 Parrish, J.T., and Curtis, R.L., 1982. Atmospheric circulation, upwelling, and organic-rich rocks in the Mesozoic and Cenozoic Eras, Palaeogeography, Palaeoclimatology, and Palaeoecology, v. 40, p. 31-66. (19f) 1983 1983-01 Ziegler, A.M., Scotese, C.R., and Barrett, S.F., 1983. Mesozoic and Cenozoic paleogeographic maps, in Tidal friction and the Earth's Rotation II, P. Broche and J. Sundermann, eds., Springer-Verlag, Berlin. (21) 1983-02 McCabe, C., Van der Voo, R., Peacor, D.R., Scotese, C.R., and Freeman, R., 1983. Diagenetic magnetite carriers ancient yet secondary remanence in some Paleozoic sedimentary carbonates, Geology v. 11, pp. 221-223. (22a) 1983-03 Scotese, C.R. and Van der Voo, R., 1983. Paleomagnetic dating of Alleghanian folding, American Geophysical Union, 1983 Spring Annual Meeting, Eos, v. 64, Issue 18, p. 218. 1983-04 Ziegler, A.M., Scotese, C.R., and Lottes, A.L., 1983. Report on Mesozoic-Cenozoic Lithofacies of China for the British Petroleum Company Limited from the Global Geology Group, University of Chicago. (22b) 1983-05 Scotese, C.R., 1983. Plate Tectonic Reconstruction Software, PALEOMAP Fortran program (Subroutines MAIN.FTN, RECON8.FTN, ADDER.FTN, ROTATE.FTN, MOLL.FTN), Department of Geophysical Science, University of Chicago, 14 pp. (22d) 1983-06 Ziegler, A.M., and Scotese, C.R., 1983. Paleogeographic Atlas Project Catalog, University of Chicago. (22e) 1983-07 Scotese, C.R., 1983. Changing face of the Earth as portrayed at 60 million year intervals from the Cambrian period to the present, p. 51, in R. Sevier, The Dynamic Earth, Scientific American, September, 1983, volume 249, number 3, p. 46 - 55. (22c) 1983-08 Parrish, J.T., Ziegler, A.M., and Scotese, C.R., 1983. Global paleogeography and paleoclimate in the Late Carboniferous, Geological Society of America, 1983, Annual Meeting, Abstracts with Programs, 15:658. 1983-09 Scotese, C.R., 1983. Illustrations in the chapter, “Discovery of Planet Earth”, on pp. 42, 47, 49, 51, and 53, in Exploring Our Living Planet, by Robert D. Ballard, National Geographic Society, Washington, D.C., 366 pp. 1983-10 Parrish, J.T., Ziegler, A.M., and Humphreville, R.G., 1983. Upwelling in the Paleozoic Era, in J. Thiede and E. Suess (editors), Coastal Upwelling: Its Sediment Record, Vol II., Plenum Press, New York, p. 573-578. (22f) 1984 1984-01 Scotese, C.R., 1984. An introduction to this volume: Paleozoic Paleomagnetism and the Assembly of Pangea, in Plate Reconstruction from Paleozoic Paleomagnetism, R. Van der Voo, C.R. Scotese, N. Bonhommet, eds. Geodynamics, v. 12, Amer. Geophys. Union, Washington, D.C. pp. 1-10. (24) 1984-02 Van der Voo, R., Peinado, J., and Scotese, C.R., 1984. A paleomagnetic reevaluation of Pangaea reconstructions, in Plate Reconstruction from Paleozoic Paleomagnetism, R. Van der Voo, C.R. Scotese, N. Bonhommet, eds. Geodynamics, v. 12, Amer. Geophys. Union, Washington, D.C., pp. 11-26. (26) 1984-03 Van der Voo, R., McCabe, and Scotese, C.R., 1984. Was Laurentia part of an Eocambrian supercontinent? in Plate Reconstruction from Paleozoic Paleomagnetism, R. Van der Voo, C.R. Scotese, N. Bonhommet, eds. Geodynamics, v. 12, Amer. Geophys. Union, Washington, D.C., pp. 131-136. (27b) 1984-04 Van der Voo, R.,Scotese, C.R., and Bonhommet, N., (editors) 1984. Plate Reconstruction from Paleozoic Paleomagnetism, Geodynamics V. 12, Amer. Geophys. Union, Washington, D.C., 136 pp. (23) 1984-05 Scotese, C.R., Van der Voo, R., Johnson, R.W., and Giles, P.S., 1984. Paleomagnetic results from the Carboniferous of Nova Scotia, in Plate Reconstruction from Paleozoic Paleomagnetism, R. Van der Voo, C.R. Scotese, N. Bonhommet, eds. Geodynamics, v. 12, pp. 63-81. (25) 1984-06 Scotese, C.R., and Lawver, L.A., 1984. Preliminary Plate Tectonic Reconstruction of the Indian Ocean at Anomaly M10, 34, 28, 13 and 5 Times, Part I, Paleoceanographic Mapping Project (POMP) Progress Report 01-0684, 34 pp. (UTIG Technical Report 49) 1984-07 Scotese, C.R., and Lawver, L.A., Sclater, J.G., and Sawyer, D., 1984. The Paleooceanographic Mapping Project (POMP): Research Goals, Methods, and Future Plans, Paleoceanographic Mapping Project (POMP) Progress Report 02-1184, 12 pp. (UTIG Technical Report 50) 1984-08 Scotese, C.R., 1984. Early Paleozoic evolution of the Circum-Pacific region, 27th International Geological Congress, abstracts, Vol. IX, Part 1, p. 48. 1984-09 Scotese, C.R., 1984. Paleozoic Basemaps, Paleoceanographic Mapping Project (POMP) Progress Report 03-0984, 22 pp. (UTIG Technical Report 51) 1984-10 Ziegler, A.M., Hulver, M.L., Lottes, A.L., and Schmactenberg, W.F., 1984. Uniformitarianism and paleoclimates: Inferences from the distribution of carbonate rocks, XXXsource?XXX (27a) 1985 1985-01 Rowley, D.B., Raymond, A., Parrish, J.T., Lottes, A., Scotese, C.R., and Ziegler, A.M., 1985. Carboniferous paleogeographic, phytogeographic, and paleoclimatic reconstructions, T.L. Phillips and B. Cecil, (eds.), Paleoclimatic controls on coal resources of the Pennsylvanian System of North America. International Journal of Coal, Geology, Volume 5, Issue 1-2, p. 7-42. (29_30) 1985-02 Scotese, C.R. and Rowley, D.B., 1985. The orthogonality of subduction: An empirical rule? Tectonophysics, 116:173-187. (31) 1985-03 McKerrow, W.S., and Scotese, C.R., 1985. The Ordovician to Devonian Development of the Iapetus Ocean, Paleoceanographic Mapping Project (POMP) Progress Report 08-0185, 30 pp. (UTIG Technical Report 55) 1985-04 Scotese, C.R., 1985. The assembly of Pangea, middle and late Paleozoic paleomagnetic results from North America, 339 p. (Ph.D. Thesis, University of Chicago) (28) pages out of order 1985-05 Scotese, C.R., Van der Voo, R., and Barrett, S.F., 1985. Silurian and Devonian base maps, Philosophical Transactions of the Royal Society of London, Series B, 309:57-77. (32) 1985-06 Rosencrantz, E., and Scotese, C.R., 1985. Reconstructions of Caribbean Stratigraphy and Tectonics: Database User’s Manual, Institute for Geophysics, University of Texas at Austin, TX, 26 pp. scan text 1985-07 Scotese, C.R., 1985. Paleomagnetic constraints on the collision of North America and Europe during the Caledonian Orogeny, American Geophysical Union, 1985 Spring Annual Meeting, Eos, v. 66, Issue 46, p. 875. 1985-08 Scotese, C.R., 1985. The Shaping of a Continent, Supplement to the National Geographic, August 1985, Vo. 168, No. 2, p. 142A. (32b) 1985-09 McCabe, C., and Scotese, C.R., 1985. Paleomagnetic Constraints on the Fit of the Continents Around the Gulf of Mexico, Paleoceanographic Mapping Project (POMP) Progress Report 07-1285, 18 pp. (UTIG Technical Report 54) 1985-10 Lawver, L.A., and Scotese, C.R., 1985. Revised Reconstruction of Gondwana, Paleoceanographic Mapping Project (POMP) Progress Report 04-0885, 16 pp. (UTIG Technical Report 52) 1985-11 Gahagan, L., Larson, R.L., and Scotese, C.R., 1985. Plate Tectonic Reconstructions of the Larson et al. (1985) Map of the Age of the World Oceans, Paleoceanographic Mapping Project (POMP) Progress Report 05-0985, 15 pp. (UTIG Technical Report 53) 1985-12 Scotese, C.R., Totterdell, J.M., Holliday, S. and Langford, R.P, 1985. Paleogeographic Mapping Software for the Intergraph Work Station. BMR-AMIRA Paleogeographic Project, Special Report, Bureau of Mineral Resources, Canberra, Australia, 136 pp. This report describes a set of programs that produces palaeocontinental reconstructions illustrating the positions of the continents during the last 600 million years and plots on these base maps lithologic information portraying the llthofacies and environments of deposition. These programs are based on the PALEOMAP software package written by C.R. Scotese, and the lithologic data illustrated on these data maps have been compiled by A.M. Ziegler and associates, as part of the Palaeogeographic Atlas Project, University of Chicago. The PALEOMAP software package was installed on the Intergraph system in the Division of Continental Geology, Bureau of Mineral Resources by C.R. Scotese, with the help of J.M. Totterdell, S. Holliday, and R.P. Langford during November of 1985.This report 1) describes the programs that comprise the PALEOMAP software package, 2) provides illustrations of the output of these programs (Table 1; Figures 2-45), 3) provides examples of the user input required to run the programs (Appendices A-D), and 4) documents both the programs (Appendices E-H) and lithologic data that were used to produce the paleogeographic lithofacies maps of Australia (Appendices I-Y). 1985-13 Lawver, L.A., and Scotese, C.R., 1985. Gondwana revisited, American Geophysical Union, American Geophysical Union, 1985 Fall Meeting, Eos, v. 66, Issue 46, p. 1073. 1985-14 Raymond, A., Parker, W.C., and Parrish, J.T., 1985. Phytogeography and paleoclimate of the Early Carboniferous, in B.H. Tiffney, editor, Geological Factors and the Evolution of Plants, Yale University Press, p. 169-222. CRS not coauthor 1985-15 Lottes, A.L., and Scotese, C.R., 1985. Plate Reconstruction Software, Paleogeographic Atlas Project, Department of Geophysical Sciences, University of Chicago, IL, 52 pp. (35b) 1985-16 Lottes, A.L., and Scotese, C.R., 1986. User’s guide to Paleogeographic Atlas Project Data and Software, Paleogeographic Atlas Project, Department of Geophysical Sciences, University of Chicago, IL, 47 pp. (35c) 1986 1986-01 Parrish, J.T., Ziegler, A.M., Scotese, C.R., Humphreville, R.G., and Kirschvink, J.L., 1986. Chapter 22, Proterozoic and Cambrian Phosphorites – Specialist Studies: Early Cambrian palaeogeography, palaeoceanography and phosphorites, in Phosphate Deposits of the World vol.1, Proterozoic and Cambrian Phosphorites, P.J. Cook & J.H. Shergold, (editors), pp. 280-294, Cambridge University Press. (34) 1986-02 Scotese, C.R. and Summerhayes, C.P., 1986. Computer model of paleoclimate to predict upwelling in the Mesozoic and Cenozoic. Geobyte, 1:28-42.(33) A computer program has been developed that models paleoclimate using a parametric approach. The program generates atmospheric pressure values and contours them to produce atmospheric pressure for past times of known land and sea distribution. Wind directions inferred from the pressure distribution can be added to the maps to show where coastal upwelling may have taken place. Organic-rich muds form in such places today, thus upwelling predictions from paleoclimate models may provide clues about the distribution of potential petroleum source rocks. These predictions proved satisfactory for the Volgian and Cenomanian, the two times for which maps of organic-rich rocks were readily available. Similar test are recommended for other time slices. The paleoclimate maps derived by the computer modeling approach use here are preliminary. Nevertheless they offer a reasonable best-guess as to the earth's climate in the past. Eventually, more sophisticated modeling techniques may provide netter results. 1986-03a Scotese, C.R., 1986. The Paleoceanographic Mapping Project Software Update: User’s Manual, Institute for Geophyics, University of Texas, Austin, TX, 69 pp. 1986-03b Scotese, C.R., 1983. In the chapter, “The Living Machine”, on pp. 45-47, in Planet Earth: The Companion to the PBS Television Series, by Jonathan Weiner, Bantam Books, February, 1986, ISBN 0-553-05096-6, 370 pp. 1986-04 Ross, M.I., and Scotese, C.R., 1986. Preliminary Tectonic Reconstructions of the Gulf of Mexico and Northern Caribbean Region, Paleoceanographic Mapping Project (POMP) Progress Report 11-0586, 34 pp. (UTIG Technical Report 58) 1986-05 Scotese, C.R., and Winn, K., The Opening of the Red Sea and Gulf of Aden: Implications for the Evolution of East Africa, Paleoceanographic Mapping Project (POMP) Progress Report 12-0586, 7 pp. (UTIG Technical Report 59 pp. 1986-06 Scotese, C.R., 1986. Phanerozoic Reconstructions: A New Look at the Assembly of Asia, Paleoceanographic Mapping Project (POMP) Progress Report 19-1286, 54 pp. (UTIG Technical Report 66) 1986-07 Scotese, C.R., Gahagan, L.M., Ross, M.I., Royer, J.Y., Nuernberg, D., Mayes, C.L., Lawver, L., Tomlins, R.L., Newman, J.S., Heubeck, C.E., Winn, J.K., Beckley, L., and Sclater, J.G., 1986. Atlas of Mesozoic and Cenozoic Plate Tectonic Reconstructions, Technical Report 90, Institute for Geophysics, University of Texas of Austin, XX pp. not sure what this is 1986-08 Scotese, C.R., 1986. Paleomagnetic dating of Alleghanian folding in the Central Appalachians, Institute for Geophysics, University of Texas, Austin, TX, 32 pp. 1986-09 Scotese, C.R., 1986. Atlas of Phanerozoic Base Maps, Technical Report 60, Institute for Geophysics, Paleoceanographic Mapping Project (POMP), University of Texas of Austin, XX pp. ???? 1986-10 McCabe, C., Van der Voo, R., and Scotese, C.R., 1986. Implications of remagnetized limestone paleomagnetic poles for Pangea, Department of Geology, Louisiana State University, Baton Rouge, LA, 18 pp. 1986-11 Scotese, C.R., and Baird, G.C., 1986. Paleomagnetic results from the Carbondale and Bond formations of the Illinois Basin (Mazon Creek), Institute for Geophysics, University of Texas, Austin, TX, 33 pp. 1986-12 Lawver, L.A., and Scotese, 1986. Review of Tectonic Models for the Evolution of the Canada Basin, Paleoceanographic Mapping Project (POMP) Progress Report 14-1086, 59 pp. (UTIG Technical Report 61) 1986-13 Scotese, C.R., 1986. Development of the Circum-Pacific Panthalassic Ocean during the Early Paleozoic, Paleoceanographic Mapping Project (POMP) Progress Report 10-0386, 9 pp. (UTIG Technical Report 57) 1986-14 Heubeck, C.E., and Scotese, C.R., 1986. Reconstruction of the Central and North Atlantic Using New Information from Satellite Altimetry, Paleoceanographic Mapping Project (POMP) Progress Report 16-1186, 13 pp. (UTIG Technical Report 63) 1986-15 Gahagan, L.M., Heubeck, C.E., Mayes, C.L., Sandwell, D.T., and Scotese, C.R., 1986. Tectonic Fabric of the Ocean Basins Derived from Satellite Altimetry, Paleoceanographic Mapping Project (POMP) Progress Report 18-1286, 7 pp. (UTIG Technical Report 65) 1986-16 Bergh, H., Lawver, L.A., and Scotese, C.R., 1986. The evolution of the plate boundary between Africa and Antarctica during the Late Jurassic and Cretaceous (Anomaly M22 to 34 Time), in W. Sager and C.R. Scotese (editors), 1986 Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, Texas A&M University, College Station, TX, April 23-25, 1986 (abstract). 1986-17 Gahagan, L.M., Scotese, C.R., and Larson, R., 1986. Plate tectonic reconstructions of the Larson et al (1985) Map of the Age of the Ocean, in W. Sager and C.R. Scotese (editors), 1986 Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, Texas A&M University, College Station, TX, April 23-25, 1986 (abstract). 1986-18 Ross, M.I., Rosencrantz, E., and Scotese, C.R., 1986. Caribbean Plate Reconstructions: New interpretation of data in the Cayman Trough, in W. Sager and C.R. Scotese (editors), 1986 Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, Texas A&M University, College Station, TX, April 23-25, 1986 (abstract). 1987 1987-01 Lawver, L. and Scotese, C.R., 1987. A revised reconstruction of Gondwana, in Gondwana Six: Structure, Tectonics, and Geophysics, American Geophysical Union, Monograph 40:17-23. (37a) Abstract: A revised reconstruction of Gondwana is presented. It is based on previous reconstructions that were geologically well constrained and utilizes marine magnetic anomalies and recent paleomagnetic results as additional constraints. Three areas of conflict, namely, the position of Madagascar, the location of India-Sri Lanka, and the overlap of the Antarctic Peninsula with the Falkland Plateau are discussed. An interactive graphics terminal was used to minimize continental overlap while reducing obvious gaps between prebreakup components. Poles and angles of rotation were determined directly from the optimal geometric fit. 1987-02 Scotese, C.R., 1987. Paleoclimate expert system that predicts coastal upwelling, American Association of Petroleum Geologists Annual Convention (abstract), AAPG Bulletin, v. 71, issue 5, p. 611. 1987-03 Ross, M.I., and Scotese, C.R., 1986. Revised Tectonic Reconstruction of the Gulf of Mexico and Northern Caribbean Region, Paleoceanographic Mapping Project (POMP) Progress Report 17-0187, 27 pp. (UTIG Technical Report 64) 1987-04 Scotese, C.R., 1987. Development of the Circum-Pacific Panthallasic Ocean during the Early Paleozoic. in Circum-Pacific Orogenic Belts and the Evolution of the Pacific Ocean Basin, J. W. Monger and J. Francheteau (editors), American Geophysical Union, Geodynamics series, v. 18, 49-57. (36) 1987-05 Heubeck, C.E., Royer, J.Y., and Scotese, C.R., 1987. Comparison of Plate Tectonic Models for the North and Central Atlantic, Paleoceanographic Mapping Project (POMP) Progress Report 20-0487, 24 pp. (UTIG Technical Report 67) 1987-06 Scotese, C.R., Lawver, L.A., Sclater, J.G., Mayes, C.L., Norton, I., and Royer, J.-Y., 1987. Plate tectonic evolution of circum-Antarctic passive margins, American Association of Petroleum Geologists Annual Convention (abstract), AAPG Bulletin, v. 71, issue 5, p. 611. 1987-07 Scotese, C.R., Ross, M.I., Lawver, L.A., Toyer, J.Y., Gahagan, L.M., Heubeck, C., Mayes, C.L., Müller, D., Savrdo J., Winn, K., and Sclater, J.G., 1987. A global model of Mesozoic and Cenozoic plate motions, 1987 Geodynamics Symposium, Silver anniversary Celebration of Plate Tectonics, Texas A&M University, College Station, TX, April. 1987-08 Müller, R.D., Scotese, C.R., and Heubeck, C.E., 1987. The Opening of the Central Atlantic: Seafloor Spreading Isochrons and Tectonic Fabric from SEASAT Altimetry, Paleoceanographic Mapping Project (POMP) Progress Report 21-0687, 15 pp. (UTIG Technical Report 68) 1987-09 Scotese, C.R., Gahagan, L.M., Ross, M.I., Royer, J.Y., Nuernberg, D., Mayes, C.L., Lawver, L., Tomlins, R.L., Newman, J.S., Heubeck, C.E., Winn, J.K., Beckley, L., and Sclater, J.G., 1987. Phanerozoic Plate Tectonic Reconstructions, Technical Report 90, Institute for Geophysics, University of Texas of Austin, 20 pp. 1987-10 Müller, R.D., Nurnberg, D.R. and Scotese, C.R., 1987. The Fit of the Continents Around the South Atlantic, Paleoceanographic Mapping Project (POMP) Progress Report 22-0787, 25 pp. (UTIG Technical Report 69) 1987-11 Lawver, L.A., Scotese, C.R., Bergh, H., Norton, I., Royer, J.Y., and Mayes, C.L., Plate tectonic evolution of the Southern Oceans: An Antarctic Perspective, 5th International Antarctic Earth Sciences Symposium, Cambridge, U.K., August 23-29, 1987. 1987-12 Royer, J.Y., Patriat, P., Bergh, H., and Scotese, C.R., 1987. Evolution of the Southwest Indian Ridge from the Late Cretaceous (Anomaly 34) to the Middle Eocene (Anomaly 20), Paleoceanographic Mapping Project (POMP) Progress Report 25-0987, 46 pp. (UTIG Technical Report 76) 1987-13 Scotese, C.R., and Ross, Malcolm I, 1987. Parametric climate modeling and coastal upwelling prediction, Geological Society of America, 1987, Annual Meeting, Phoenix, AZ, Ocotber 26-69, Abstracts with Programs, 19:836. 1987-14 Gahagan, L.M., Royer, J.Y., Scotese, C.R., Sandwell, D.T., Winn, J.K., Tomlins, R.L., Ross, M.I., Newman, J.S., Müller, R.D., Mayes, C.L., Lawver, L.A., and Heubeck, C.E., 1987. Tectonic Fabric Map of the Ocean Basins from Satellite Altimetry Data, G.S.A Annual Meeting, Phoenix, Arizona, October 26-69, 1987. 1987-15 Winn, K., and Scotese, C.R., 1987. PALEOMAP (Plate Tectonic Mapping Program): A User’s Manual, Paleoceanographic Mapping Project (POMP) Progress Report 38-1287, 20 pp. (UTIG Technical Report 89) 1987-16 Scotese, C.R., 1987. Abstracts Submitted by POMP Members in 1987, Paleoceanographic Mapping Project (POMP) Progress Report 30-1287, 11 pp. (UTIG Technical Report 81) 1987-17 Gahagan, L.M. and Scotese, C.R., 1987. Appendices, Paleoceanographic Mapping Project (POMP) Progress Report 35-1287, 38 pp. (UTIG Technical Report 86) 1987-18 Gahagan, L.M., Royer, J.Y., Sandwell, D.T., Scotese, C.R., Winn, J.K., Tomlins, R.L., Ross, M.I., Newman, J.S., Müller, R.D., Mayes, C.L., Lawver, L.A., and Huebeck, C.E., 1987. Tectonic Fabric Map of the Ocean Basins from Satellite Altimetry Data, Paleoceanographic Mapping Project (POMP) Progress Report 32-1287, 32 pp. (UTIG Technical Report 83) 1987-19 Nurnberg, D., Müller, R.D., and Scotese, C.R., 1987. The Tectonic Evolution of the South Atlantic from Late Jurassic to Present, Paleoceanographic Mapping Project (POMP) Progress Report 27-1287, 41 pp. (UTIG Technical Report 78) 1987-20 Müller, R.D., and Scotese, C.R., 1987. The Tectonic Development of the North Atlantic: Revised Seafloor Spreading Isochrons and Tectonic Fabric Map from SEASAT Altimetry, Paleoceanographic Mapping Project (POMP) Progress Report 26-1287, 49 pp. (UTIG Technical Report 77) 1987-21 Winn, K., and Scotese, C.R., 1987. Paleoceanographic Mapping Project Digitizing Software: A User’s Manual, Paleoceanographic Mapping Project (POMP) Progress Report 37-1287, 64 pp. (UTIG Technical Report 88) 1987-22 Lawver, L.A., Royer, J.Y., Sandwell, D.T., and Scotese, C.R., 1987. Evolution of the Antarctic continental margins, Paleoceanographic Mapping Project (POMP) Progress Report 31-1287, 20 pp. (UTIG Technical Report 82) 1987-23 Gahagan, L.M., Larson, R.L., and Scotese, C.R., 1987. Plate Tectonic Reconstructions of the Cretaceous and Cenozoic Ocean Basins, Paleoceanographic Mapping Project (POMP) Progress Report 34-1287, 45 pp. (UTIG Technical Report 85) 1987-24 Winn, K., and Scotese, C.R., 1987. MEGAPOLY: A User’s Manual, Paleoceanographic Mapping Project (POMP) Progress Report 36-1287, 38 pp. (UTIG Technical Report 87) 1987-25 Scotese, C.R., and Winn, K., 1987. Phanerozoic Paleogeographic Maps, Paleoceanographic Mapping Project (POMP) Progress Report 33-1287, 31 pp. (UTIG Technical Report 84) 1988 1988-01 Scotese, C.R. and Sager, W.W., 1988. 8th Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, Tectonophysics, v. 155, issues 1-4, pp. 1-399. (38) 1988-02 Scotese, C.R., Gahagan, L.M., and Larson, R.L., 1988. Plate tectonic reconstructions of the Cretaceous and Cenozoic ocean basins, in 8th Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, C.R. Scotese & W.W. Sager (editors), Tectonophysics, 155:261-283. (42a) 1988-03 Royer, J.-Y., Patriat, P., Bergh, H., and Scotese, C.R., 1988. Evolution of the southwest Indian Ridge from the Late Cretaceous (anomaly 34) to the Middle Eocene (anomaly 20), in 8th Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, C.R. Scotese & W.W. Sager (editors), Tectonophysics, 155:235-260. (41) 1988-04 Gahagan, L.M., Scotese, C.R., Royer, J.Y., Sandwell, D.T., Winn, K., Tomlins, R., Ross, M.I., Newman, J.S., Mueller, D., Mayes, C.L., Lawver, L.A. and Heubeck, C.E., Tectonic fabric map of the ocean basins from satellite altimetry data, in 8th Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, C.R. Scotese & W.W. Sager (editors), Tectonophysics, 155:1-26. (39) 1988-05 Scotese, C.R. and Denham, C.R., 1988. User’s manual for Terra Mobilis™: Plate Tectonics for the Macintosh®. (42b) 1988-06 Müller, R.D., Scotese, C.R., and Sandwell, D.T., 1988. The Opening of the Central and North Atlantic: Revised Seafloor Spreading Isochrons and Tectonic Map from Geosat Data, Paleoceanographic Mapping Project (POMP) Progress Report 39-0888, 38 pp. (UTIG Technical Report 91) 1988-07 Scotese, C.R., Gahagan, L.M., Royer, J.-Y., Mueller, R.D., Ross, M.I., Nurnberg, D., Mayes, C.L., Lawver, L.A., Tomlins, R., and Beckley, L., 1988. Phanerozoic plate tectonic reconstructions, Geological Society of America 1988 Centennial Celebration, Abstracts with Programs, v. 20, Issue 7, p. 229. 1988-08 Mueller, R.D., Beckley, L., Gahagan, L.M., Lawver, L.A., Mayes, C.L., Nurnberg, D., Ross, M.I., Royer, J.-Y., Sclater, J.G., Scotese, C.R., and Tomlins, R.L., 1988. A model for global plate motions from the Jurassic to present-day, Geological Society of America 1988 Centennial Celebration, Abstracts with Programs, v. 20, Issue 7, p. 62. 1988-09 Ross, M.I. and Scotese, C.R., 1988. A hierarchical tectonic model of the Gulf of Mexico and Caribbean region, in 8th Geodynamics Symposium, Mesozoic and Cenozoic Plate Reconstructions, C.R. Scotese & W.W. Sager (editors), Tectonophysics, 155:139-168. (40) 1989 1989-01 Bally, A.W., Scotese, C.R., and Ross, M.I., North America: Plate tectonic setting and tectonic elements, in A.W. Bally and A.R. Palmer, (editors), The Geology of North America; An Overview, Decade of North American Geology, The Geology of North America, Volume A., 1-15. (43a) 1989-02 J.Y. Royer, L.M. Gahagan, L.A. Lawver, C.L. Mayes, D. Nurnberg, D.T. Sandwell, Christopher Robert Scotese, 1989. A Tectonic Chart for the Southern Oceans from Geosat Altimetry Data, Paleoceanographic Mapping Project (POMP) Progress Report 53-0389, 24 pp. 1989-03 R.D. Müller, L. Beckley, L.M. Gahagan, L.A. Lawver, C.L. Mayes, D. Nurnberg, M.I. Ross, J.Y. Royer, J.G. Sclater, Christopher Robert Scotese, R.L. Tomlins, D.T. Sandwell, T.Y. Lee, 1989. POMP Abstracts Presented at Meetings in 1988, Paleoceanographic Mapping Project (POMP) Progress Report 56-0389, 5 pp. 1989-04 Carroll, L.P., 1989. The Paleomap Project, The World & I, Natural Science, March, 1989, p. 273-291. (43b) 1989-05 Scotese, C. R., and Ross, M.I., 1989. Paleogeographic reconstructions using three-dimensional computer graphics,1989 AAPG Annual Convention, April 23-26, San Antonio, TX. 1989-06 Lawver, L.A., Gahagan, L.M., Dalziel, I.W.D., Sandwell, D.S., Mayes, C.L., Royer, J.-Y., and Scotese, C.R., 1989. Paleozoic to Recent Gondwanaland and its breakup, International Geological Congress, Abstracts, Vol. 28, p. 2.266. 1989-07 Lawver, L.A., Gahagan, L.M., Dalziel, I.W.D., Sandwell, D.S., Mayes, C.L., Royer, J.-Y., and Scotese, C.R., 1989. The fragmentation of Gondwanaland, International Geological Congress, Abstracts, Vol. 28, 2, p. 2.265. 1989-08 CRS Swiss Academy of Sciences talk 1990 1990-01 Lawver, A. and Scotese, C.R., 1990. A review of tectonic models for the evolution of the Canada Basin, Chapter 31, in A. Grantz, L. Johnson, and J.F. Sweeney, (editors), The Arctic Ocean Region, Decade of North American Geology, volume L, pp. 593-618, Geological Society of America, Boulder, CO. (45) 1990-02 Scotese, C.R., Tyrell, W.W., Jr., and Maher, K.A., 1990. The tectonic development of south-central Asia and the paleogeographic setting of its hydrocarbon resources, AAPG Annual Convention with DPA/EMD divisions and SEPM, America Association of Petroleum Geologists Bulletin, v. 74, issue 5, p. 760. 1990-03 McKerrow, W.S. and Scotese, C.R. (editors),1990. Paleozoic Paleogeography and Biogeography, Geological Society of London, Memoir 12, 435 p. (45) 1990-04 Scotese, C.R. and McKerrow, W.S., 1990. Revised world maps and introduction, in Paleozoic Paleogeography and Biogeography, W.S. McKerrow and C.R. Scotese (editors), Geological Society of London, Memoir 12, pp. 1-21. (49a) 1990-05 Royer, J.Y., Gahagan, L.M., Lawver, L.A., Mayes, C.L., Nurnberg, D., Sandwell, D.T., and Scotese, C.R., 1990. A tectonic chart for the southern oceans derived from GEOSAT altimetry data, in AAPG Studies in Geology, Antarctica as an exploration frontier, hydrocarbon potential, geology, and hazards, Bill St. John (editor), Vol. 31, pp. 89-99. (47) Abstract: Presented is a new tectonic fabric map of the southern ocean south of 45S, derived from Geosat altimeter profiles and published bathymetric charts and magnetic anomaly picks. The interpretation of the Geosat data is based on an analysis of the first derivative of the geoid profiles (i.e., vertical deflection profiles). To improve the accuracy and resolution of the vertical deflection profiles, 22 repeat cycles from the first year of the Geosat/Exact Repeat Mission (Geosat/ERM) were averaged. At wavelengths less than about 200 km, the vertical deflection is highly correlated with sea-floor topography and thus reveals major features in areas that were previously unsurveyed. The density of the Geosat data is greatest in the high latitudes where lineated bathymetric features such as fracture zones, spreading ridges, trenches, and rifted margins stand out. To construct the tectonic fabric chart, the Geosat data are analyzed in combination with available shipboard bathymetric data and magnetic anomaly identifications. 1990-06 Scotese, C.R. and Barrett, S.F., 1990. Gondwana's movement over the South Pole during the Paleozoic: evidence from lithologic indicators of climate, in Paleozoic Paleogeography and Biogeography, W.S. McKerrow and C.R. Scotese (editors), Geological Society of London, Memoir 12, pp. 75-85.(48) Abstract: A statistical technique is described that uses the geographical distribution of lithological indicators of climate (carbonates, evaporites, coals and tillites) to estimate the past position of the geographic pole. This technique was used to estimate the movement of the South Pole across the supercontinent of Gondwana during the Palaeozoic. Results indicate that during the Cambrian and Early Ordovician the South Pole was located adjacent to northwestern Africa. The pole moved into the Amazon Basin during the Late Ordovician and into south-central Argentina during the Silurian. Throughout the Devonian and Early Carboniferous the pole moved slowly from a location in southern Argentina to a position near the south coast of Africa. From the Late Carboniferous and into the Permian the South Pole swung eastward across central Antarctica. The Early Palaeozoic and Late Palaeozoic portions of the palaeoclimatically determined APW (apparent polar wander) path are in good agreement with available palaeomagnetic data. The Middle Palaeozoic portion of the palaeoclimatically determined APW path agrees better with the palaeomagnetic data that places the South Pole in southern Argentina, than with the palaeomagnetic results that place the Devonian pole in central Africa. 1990-07 Scotese, C.R., and McKerrow, W.S., 1990. Ordovician Plate Tectonic Reconstructions, PALEOMAP Progress Report 03-0390, Department of Geology, University of Texas at Arlington, Texas, p 271-282. (UTIG 141) 1990-08 Scotese, C.R., Maher, K.A., and Tyrell, W.W., 1990. The tectonic and paleogeographic development of south-central Asia, Geological Society of America, Northeastern Section, 25th Annual Meeting, Abstracts with Programs, v. 22, Issue 2, p. 68. 1990-09 McKerrow, W.S., and Dewey, J.F., and Scotese, C.R., 1990. The Ordovician and Silurian Development of the Iapetus Ocean, PALEOMAP Progress Report 05-0890, Department of Geology, University of Texas at Arlington, Texas, p 165-178. (UTIG 143) 1990-10 Cocks, L.R.M. and Scotese, C.R., The Global Biogeography of the Silurian Period, PALEOMAP Progress Report 04-0890, Department of Geology, University of Texas at Arlington, Texas, p 109-122. (UTIG 142) 1990-11 Thompson, A.B., Christensen, U., England, P.C., Spakman, W., Kissling, E., Pavonia, N., Tarduno, J.A., Ziegler, P.A., Scotese, C.R., and Rowley, D.B., 1990. Mantle structure and geotectonics: Abstracts of the Annual Meeting of the Swiss Academy of Sciences, Eclogae Geologicae Helvetiae, Vol. 83, Issue 1, p. 208-216, Birkhaeuser Verlag, Basel, Switzerland. 1990-12 Scotese, C.R., 1990. Phanerozoic plate tectonics reconstructions, insights into the driving mechanism of plate tectonics, Bulletin, Houston Geological Society, 32 (9), p. 10.1990-12 1990-13 Scotese, C.R., 1990. Atlas of Phanerozoic Plate Tectonic Reconstructions, PALEOMAP Progress 01-1090a, Department of Geology, University of Texas at Arlington, Texas, 57 pp (also UTIG 139) (49d) 1990-14 Scotese, C.R., Van der Voo, R., Mueller, R.D., and McKerrow, W.S., 1990. Phanerozoic plate tectonic reconstructions: Results of the PALEOMAP Project, Geological Society of America, 1990 Annual Meeting, Abstracts with Programs, v. 22, Issue 7, pp. 229-230. 1990-15 Scotese, C.R., 1990. Text for Atlas of Phanerozoic Plate Tectonic Reconstructions, PALEOMAP Progress 01-1090b, Department of Geology, University of Texas at Arlington, Texas, 35 pp. also (UTIG 139) (49b) 1990-16 Burkart, B., And Scotese, C.R., 1990. The Orizaba fault zone: Link between the Mexican volcanic belt and strike-slip faults of northern Central America, American Geophysical Union, 1990 Fall Meeting, EOS, Transactions of the American Geophysical Union, v. 71, issue 43, p. 1559. 1990-17 Ziegler, A.M., 1990. Paleogeographic Atlas Project, First Annual Meeting, June 21 -22, 1990, Department of Geophysical Sciences, University of Chicago, Chicago, IL, 105 pp. (49c) 1991 1991-01 Cocks, L.R.M. and Scotese, C.R., 1991. The global biogeography of the Silurian period, in Bassett, M.G. (editor), The Murchison Symposium, Special Paper in Palaeontology v. 44, Geol. Society of London, pp. 109-122. (50a) 1991-02 McKerrow, W.S., Dewey, J.F., and Scotese, C.R., 1991. The Ordovician and Silurian development of the Iapetus Ocean, in Bassett, M.G. (editor), The Murchison Symposium, Special Papers in Palaeontology 44:165-178. (52) 1991-03 Lawver, L.A., Royer, J.Y., Sandwell, D. T., and Scotese, C.R., 1991. Evolution of the Antarctic continental margins, in Proceedings of the 5th International Antarctic Earth Science Symposium, August 23-29, 1987, Cambridge, U.K., M.R.A. Thompson, J.A. Crame, and J.W. Thomson (editors), pp. 533-539. (50b) Abstract: With the exception of the Pacific-facing margin of West Antarctica between Thurston I. and the tip of the Antarctic Peninsula, all of the continental margins of Antarctica are either rifted passive margins or sheared transform margins. The exception was a convergent margin where subduction was active from before the break-up of Gondwana until very recently. Starting in the southwestern Weddell Sea, which rifted as part of a back-arc basin connected with Middle-Late Jurassic back-arc spreading in the Rocas Verdes Basin of southern South America, the continental margins of Antarctica seem to young clockwise. A sheared margin along the Explora Escarpment between 25 and 10W connected the southwestern Weddell Sea rifting with contemporaneous rifting in the Mozambique Basin. This resulted in a Middle Jurassic rifted passive margin along Dronning Maud Land. East of the Gunnerus Ridge at 35E, Sri Lanka and India rifted off of Antarctica some time between 127 and 118 Ma. Rifting between Australia and Antarctica, stretching in the Ross Sea embayment and rifting between the Campbell Plateau-Chatham Rise and Marie Byrd Land, all started at about 95 Ma. Active subduction ceased about 4 Ma ago off the South Shetlands Is. 1991-04 Scotese, C.R., 1991. Jurassic and Cretaceous Plate Tectonic Reconstructions, Palaeogeography, Palaeoecology, and Palaeoclimatology, v. 87, p. 493-501. (53) 1991-05 Scotese, C.R., 1991. Collection of Abstracts Presented at Geological Meetings & Symposia during 1991. PALEOMAP Progress Report 07-0291, Department of Geology, University of Texas at Arlington, Texas, 23 p (UTIG 145) find meetings for some of the abstracts 1991-06 Scotese, C.R. and McKerrow, W.S., 1991. Ordovician plate tectonic reconstructions, in Advances in Ordovician Geology, C.R. Barnes & S.H. Williams (editors), Fifth International Symposium on the Ordovician, Geological Survey of Canada Paper 90-9, p.271-282. (51) 1991-07 Scotese, C.R., and Scotese, R.J., 1991. Slide Set of Phanerozoic Paleogeographic Maps, PALEOMAP Progress Report 08-0691, Department of Geology, University of Texas at Arlington, Texas, 16 color slides. 1991-08 Scotese, C.R., 1991. Paleogeographic and plate tectonic reconstructions of Pangea, 1991 Annual Meeting Geological Society of America, Abstracts with Programs, v. 23, Issue 5, p. 28. 1991-09 Scotese, C.R., 1991. Continental Drift Flip Book, 4th edition, PALEOMAP Project, Arlington, TX, 49 pp. 1991-10 McKerrow, W.S., Scotese, C.R., and Brasier, M.D., Early Cambrian Continental Reconstructions, PALEOMAP Progress Report 02-0591, Department of Geology, University of Texas at Arlington, Texas, 33 pp. (UTIG 140) 1991-11 Scotese, C.R., 1991. Jurassic and Cretaceous Plate Tectonic Reconstructions, PALEOMAP Progress Report 06-0291, Department of Geology, University of Texas at Arlington, Texas, p 1-9. (UTIG 144) 1992 1992-01 McKerrow, W.S., Scotese, C.R., and Brasier, M.D., 1992. Early Cambrian Continental Reconstructions, Journal of the Geological Society of London, 149: 599-606. (54) 1992 -02 Waters, T., 1992., Greetings from Pangaea, Discover Magazine, February, 1992, volume 13, number 2, p. 38-43. 1992-03 Lowry, C., and Scotese, C.R., 1992. Digitizing Software: A User's Manual, PALEOMAP Progress Report 13-0492, Department of Geology, University of Texas at Arlington, Texas, 50 p. (55g) 1992-04 not used 1992-05 Scotese, C.R., and Lowry, C., 1992. PALEOMAP Program: A User's Manual, PALEOMAP Progress Report 10-0492, Department of Geology, University of Texas at Arlington, Texas, 12 p. (55d) pages out of order 1992-06 Scotese, C.R., and Lowry, C., 1992. PALEOMAPPER Program for the SUN Workstation: A User’s Manual, PALEOMAP Progress Report 11-0592, Department of Geology, University of Texas at Arlington, Texas, 14 p. (55e) 1992-07 Ross, M.I. and Scotese, C.R., 1992. Paleogeographic Information System/Mac (PGIS/Mac), version 1.3, A User’s Manual, PALEOMAP Progress Report 09-0592, Department of Geology, University of Texas at Arlington, Texas, p 1-33. (55c) 1992-08 Lowry, C., and Scotese, C.R., 1992. User's Manual for POLY_INOUT, PALEOMAP Progress Report 14-0692, Department of Geology, University of Texas at Arlington, Texas, 10 p. 1992-09 Scotese, C.R., 1992. Plate Tectonic & Paleogeographic Evolution of the Gulf of Mexico & Caribbean Region, PALEOMAP Progress Report 32-0692, Department of Geology, University of Texas at Arlington, Texas, 2 p and 9 slides. 1992-10 Lowry, C. and Scotese, C.R., 1992. MEGAPOLY: A Simple Data Management Program User’s Manual, PALEOMAP Progress Report 12-0692, Department of Geology, University of Texas at Arlington, Texas, 16 p. (55f) 1992-11 Bocharova, N.Yu. and Scotese, C.R., 1992. Suture Map of the CIS & Preliminary Plate Tectonic Reconstructions, PALEOMAP Progress Report 27-0692, Department of Geology, University of Texas at Arlington, Texas, 19 pp. (55j) 1992-12 Scotese, C.R., and Golonka, J., 1992. Slide Set of Paleogeographic Atlas, PALEOMAP Progress Report 21-0692, Department of Geology, University of Texas at Arlington, color slides. 1992-13 Scotese, C.R., and Golonka J. 1992. Paleogeographic Atlas, PALEOMAP Progress Report 20-0692, Department of Geology, University of Texas at Arlington, Texas, 34 p. (55b) 1992-14 Walsh, D.B., and Scotese, C.R., 1992. Mesozoic Paleogeographic Evolution of East Africa & the Western Indian Ocean, PALEOMAP Progress Report 30-0692, Department of Geology, University of Texas at Arlington, Texas, 7 pp. and 6 slides. 1992-15 Scotese, C.R., 1992. Phanerozoic paleogeographic, plate tectonic, and paleoclimatic reconstructions, Fifth North American Paleontological Convention, Special Publication, v. 6, p. 263. 1992-16 Walsh, D.B., and Scotese, C.R., 1992. Universal Map Digitizing Program (UMDP): A User’s Manual, PALEOMAP Progress Report 26-1092, Department of Geology, University of Texas at Arlington, Texas, 7 pp. (55i) 1992-17 Walsh, D.B., and Scotese, C.R., 1992. Cretaceous Paleogeographic Evolution of the South Atlantic, PALEOMAP Progress Report 31-1092, Department of Geology, University of Texas at Arlington, Texas, 10 p. add slides 1992-18 Bocharova, N.Yu. and Scotese, C.R., 1992. Paleomagnetic Analysis Programs: A User's Manual, PALEOMAP Progress Report 25-1092, Department of Geology, University of Texas at Arlington, Texas, 10 pp. (55l) 1992-19 Scotese, C.R., Otto-Bliesner, B. and Becker, N., 1992. Phanerozoic Paleoclimatic Simulations, PALEOMAP Progress Report 35-1092, Department of Geology, University of Texas at Arlington, Texas, 22 p. use color scans 1992-20 Zonenshain, L.P., Bocharova, N.Yu., Scotese, C.R., Kononov, M., and Pristavakina, E.I., 1992. Late Paleozoic and Early Mesozoic plate tectonic reconstructions of Russia and adjacent regions, Geological Society of America 1992 Annual Meeting, Abstracts with Programs, 24:186. 1992-21 Scotese, C.R., and Raymond, A.L., 1992. Carboniferous paleogeographic and paleoclimatic reconstructions, Geological Society of America, 192, Annual Meeting, Abstracts with Programs, 24:30. 1992-22 Walsh, D.B., and Scotese, C.R., 1992. Paleogeographic evolution of eastern Africa and the western Indian Ocean, Geological Society of America 1992 Annual Meeting, Abstracts with Programs, 24:190. 1992-23 Burkart, B., Scotese, C.R., and Moreno, G., 1992. The Orizaba Fault zone: Re-interpretation of structures along the western margin of the Isthmus of Tehuantepec in Veracruz and Chiapas states, Mexico, Geological Society of America, 1992, Annual Meeting, Abstracts with Programs, 24:5. 1992-24 Kraus, J.U., and Scotese, C.R., 1992. Paleogeographic evolution of the northern margin of Australia, Geological Society of America, 1992, Annual Meeting, Abstracts with Programs, 24:185. 1992-25 Scotese, C.R., 1992. Phanerozoic paleogeographic and plate tectonic reconstructions, Geological Society of America, 1992, Annual Meeting, Abstracts with Programs, 24:45. 1992-26 Worsley, T.R., Moore, T.L., Scotese, C.R., and Fraticelli, C.M., 1992. Phanerozoic paleogeography, CO2, and global climate, Geological Society of America 1992 Annual Meeting, Abstracts with Programs, 24:268. 1993-27 Bocharova, N. Yu., Scotese, C.R., and Van der Voo, R., 1992. Global apparent polar wander paths in a hot spot reference frame, Geological Society of America, 1992, Annual Meeting, Abstracts with Programs, 24:80. 1992-28 Ross, M.I., Scotese, C.R., and Otto-Bliesner, B., 1992. Phanerozoic paleoclimatic simulations: A comparison of the parametric climate model and the low resolution climate model, Geological Society of America, 1992, Annual Meeting, Abstracts with Programs, 24:190. 1992-29 Scotese, C.R., and Becker, N., 1992. Computer animation of Phanerozoic plate motions, Geological Society of America, 1992, Annual Meeting, Abstracts with Programs, 24:150. 1992-30 Bocharova, N.Yu., and Scotese, C.R., 1992. 3D Geological Model of the Timan-Pechora Basin, PALEOMAP Progress Report 29-1192, Department of Geology, University of Texas at Arlington, Texas, 120 pp. (55k) 1992-31 Worsley, T.R., Moore,T., Fraticelli, C., and Scotese, C.R., 1992. Phanerozoic CO2 levels and Global Temperatures Inferred from Changing Paleogeography, PALEOMAP Progress Report 22-1192, Department of Geology, University of Texas at Arlington, Texas, 55 pp. 1992-32 Scotese, C.R., 1992. Phanerozoic Plate Tectonic Reconstructions, PALEOMAP Progress Report 36-1292, Department of Geology, University of Texas at Arlington, Texas, 38 p. (56f) 1992-33 Scotese, C.R., 1992. User’s Manual for ROT_BUILDER, Plate Model Builder, PALEOMAP Progress Report 18-1292, Department of Geology, University of Texas at Arlington, Texas . 1992-34 Ross, M.I., And Scotese, C.R., 1992. User's Manual for PALEOCLIMATE Modeling Software, PALEOMAP Progress Report 16-1292, Department of Geology, University of Texas at Arlington, Texas. 1992-35 Walsh, D.B., and Scotese, C.R., 1992. PALEOMAP-PC Plate Tectonic Reconstruction Program for the IBM-PC: User’s Manual, PALEOMAP Progress Report 24-1292, Department of Geology, University of Texas at Arlington, Texas, 8 pp. 1992-36 Walsh, D.B., and Scotese, C.R., 1992. LITHPLOT Lithofacies Plotting Software: A User's Manual, PALEOMAP Progress Report 17-1292, Department of Geology, University of Texas at Arlington, Texas, 19 p (55h) 1992-37 Scotese, C.R., and Van der Voo, R., 1992. A global apparent polar wander path, American Geophysical Union 1992 Fall Meeting, EOS, Transactions of the American Geophysical Union, v. 73, issue 14, p. 88-89. 1992-38 Bocharova, N. Yu., Scotese, C.R., and Van der Voo, R., 1992. Mesozoic and Paleozoic global apparent polar wander paths, American Geophysical Union 1992 Fall Meeting, EOS, Transactions of the American Geophysical Union, v. 73, issue 43, p. 151. 1992-39 Scotese, C.R., and Langford, R. P., 1992. Pangea and the Paleogeography of the Permian, PALEOMAP Progress Report, 34-1292, Department of Geology, University of Texas at Arlington, Texas, 34 p. 1992-40 Scotese, C.R., 1992. Paleoclimate reconstructions on pp. 62-67, in Allman, W.F., and Wagner, B., Climate and the Rise of Man, U.S. News & World Report, June 8, 1992, vol. 112, No. 22. 1993 1993-01 Kraus, J.U., Scotese, C.R., Boucot, A.J., and Chen Xu, 1993. Lithologic Indicators of Climate: Preliminary Report, PALEOMAP Progress Report 33-0193, Department of Geology, University of Texas at Arlington, Texas, 16 p. 1993-02a Kraus, J.U. and Scotese, C.R., 1993. POLY_MAKER: A User’s Guide, PALEOMAP Progress Report 15-0193, Department of Geology, University of Texas at Arlington, Texas, 7 pp. 1993-02b Kraus, J.U., Scotese, C.R., Van der Voo, R., and Bocharova, N.Y., 1993. Global Paleomagnetic Data File, PALEOMAP Progress Report 39-0193, Department of Geology, University of Texas at Arlington, Texas, 53 p. (56g) 1993-03 Bocharova, N.Y., Scotese, C.R., and Natapov, L.M., 1993. Paleogeography of the North Caspian Basin, PALEOMAP Progress Report 28-0193, Department of Geology, University of Texas at Arlington, Texas, 39 p. (56e) 1993-04 Kraus, J.U., 1993. Paleogeographic Evolution of the Northwestern Australian Margin, PALEOMAP Progress Report 41-0193, Department of Geology, University of Texas at Arlington, Texas, 10 p., 3 - 35mm slides. 1993-05 Otto-Bliesner, B., and Scotese, C.R., 1993. The Global water cycle during the early Phanerozoic (570-245 millions years ago), in Fourth Symposium on Global changes Studies, Jan. 17-22, Anaheim, 1993, CA. 1993-06 Scotese, C.R., and Nie Shangyou, 1993. The Assembly of Asia: Preliminary Maps, PALEOMAP Progress Report 62-0293, Department of Geology, University of Texas at Arlington, Texas, 13 p. (56q) 1993-07 Scotese, C.R., 1993. Plate Tectonic Reconstructions and Global Paleogeography: the last 600 Million Years, Conference on Plate Tectonics, held at Southern Methodist University, February 27, 1993. 1993-08 Scotese, C.R., and Becker, N.C., 1993. Computer Animations of the PALEOMAP Project, PALEOMAP Progress Report 53-0693, Department of Geology, University of Texas at Arlington, Texas, 1p. (56l) 1993-09 Scotese, C.R., 1993. Late Precambrian and Paleozoic Paleogeography, in Stratigraphic Record of Global Change, 1993 SEPM Meeting, Penn State University, State College, PA, August 8-12, 1993, P. 11. 1993-10 Walsh, D.B., and Scotese, C.R., 1993. PMAP-ZMAP & PMAP-ARC Programs to convert PALEOMAP data into ZMAP and ARC-INFO formats, PALEOMAP Progress Report 59-0693, Department of Geology, University of Texas at Arlington, Texas, 5 p. 1993-11 Walsh, D.B., and Scotese, C.R., 1993. PALEOMAP PC: plate tectonic reconstructions on IBM compatible computers. Geological Society of America, Northeastern Section, 27th Annual Meeting, Abstracts with Programs, v. 25, Issue 1, pp. 44-45. 1993-12 Walsh, D.B., and Scotese, C.R., 1993. Manual for IBM Progam: PALEOMAP PC v.1.1, PALEOMAP Progress Report 48-0693, Department of Geology, University of Texas at Arlington, Texas, 17 p. (56a) add cover 1993-13 Scotese, C.R., McKerrow, W.S. and Nance, D. 1993. Late Precambrian Plate Tectonic Reconstructions (800-600 Ma), PALEOMAP Progress Report 61-0793, Department of Geology, University of Texas at Arlington, Texas, 6 p. (56p) 1993-14 Murphy, J. B., Nance, R. D., Worsley, T. R., and Scotese, C.R., 1993. Pangea vs. Rodinia: Tectonic Signatures and Orogenesis, in Carboniferous to Jurassic Pangea, first international symposium, B. Beauchamp, A. Embry, and D. Glass (editors), Canadian Society of Petroleum Geologists, (abstract), Calgary, AB, Canada, p. 219. 1993-15 Kraus, J. U., and Scotese, C.R., 1993. Late Paleozoic through Jurassic tectonic and paleogeographic evolution of northwestern Australia, in Carboniferous to Jurassic Pangea, first international symposium, B. Beauchamp, A. Embry, and D. Glass (editors), Canadian Society of Petroleum Geologists, (abstract), Calgary, AB, Canada, p. 172. 1993-16 Boucot, A. J., Chen, X., Kraus, J. U., and Scotese, C.R., 1993. Climatically sensitive sediments and Pangeaic paleogeography, in Carboniferous to Jurassic Pangea, first international symposium, B. Beauchamp, A. Embry, and D. Glass (editors), Canadian Society of Petroleum Geologists, (abstract), Calgary, AB, Canada, p. 32. 1993-17 Scotese, C.R., Walsh, D. B., Kraus, J. K., and Bocharova, N.Yu., 1993. Plate Evolution of Pangea from the Late Paleozoic to the Jurassic, in Carboniferous to Jurassic Pangea, first international symposium, B. Beauchamp, A. Embry, and D. Glass (editors), Canadian Society of Petroleum Geologists, (abstract), Calgary, AB, Canada, p. 274. 1993-18 Worsley, T.R., Nance, R. D., Murphy, J. B., and Scotese, C.R., 1993. Pangea vs. Rodinia: paleogeography, climate and life, in Carboniferous to Jurassic Pangea, First International Symposium, B. Beauchamp, A. Embry, and D. Glass (editors), Canadian Society of Petroleum Geologists, (abstract), Calgary, AB, Canada, p. 345. 1993-19 Golonka, J., Scotese, C.R., and Ross, M. I. 1993. Phanerozoic paleoclimatic modeling maps, in Carboniferous to Jurassic Pangea, First International Symposium, B. Beauchamp, A. Embry, and D. Glass (editors), Canadian Society of Petroleum Geologists, (abstract), Calgary, AB, Canada, p. 114. 1993-20 Kraus, J.U., Boucot, A.J., and Scotese, C.R., 1993. Carboniferous through Jurassic Lithological Indicators of Climate, PALEOMAP Progress Report 43-0893, Department of Geology, University of Texas at Arlington, Texas, 16 p. 1993-21 Stephens, S., Walsh, D.B., Kraus, J.U., and Scotese, C.R., 1993. Sedimentary Basins Datafile, PALEOMAP Progress Report 52-0893, Department of Geology, University of Texas at Arlington, Texas, 3 p. 1993-22 Kraus, J.U. and Scotese, C.R., 1993. Tectonic Evolution of New Guinea and Surrounding Areas, PALEOMAP Progress Report 44-0893, Department of Geology, University of Texas at Arlington, Texas, 71 p. 1993-23 Golonka, J., Ross, M.I., and Scotese, C.R., 1993. Atlas of Paleoclimatic Reconstructions (0-600 Ma), PALEOMAP Progress Report 60-0893, Department of Geology, University of Texas at Arlington, Texas, 30 p. 1993-24 Scotese, C.R., 1993. Late Precambrian and Paleozoic paleogeography, 1993 SEPM Meeting. Stratigraphic Record of Global Change, Society for Sedimentary Geology, (abstract only). 1993-25 Bertrand, G. and Scotese, C.R., 1993. Plate Tectonic Reconstructions of Southeast Asia (0-40 Ma), PALEOMAP Progress Report 55-0993, Department of Geology, University of Texas at Arlington, Texas, 30 p. (56m) 1993-26 Ross, M.I., and Scotese, C.R., 1993. Installation Tips for PGIS-UNIX, PALEOMAP Progress Report 47-0993, Department of Geology, University of Texas at Arlington, Texas, 6 p. (56j) 1993-27 Scotese, C.R., Kraus, J., and Boucot, A. J., 1993. Distribution of salt basins through time, A.A.P.G. Hedberg Research Conference on Salt Tectonics, Bath England, September 13-17, 1993. 1993-28 Kraus, J.U. and Scotese, C.R., 1993. Permian-Cretaceous Paleogeographic Evolution of the NW Australian Margin, PALEOMAP Progress Report 45-1093, Department of Geology, University of Texas at Arlington, Texas, 25 p. 1993-29 Kraus, J.U., and Scotese, C.R., 1993. SYMBOL_GENERATOR: A User’s Guide, PALEOMAP Progress Report 23-1193, Department of Geology, University of Texas at Arlington, Texas, 7 p. (56d) 1993-30 Scotese, C.R., 1993. Revised Paleogeographic Reconstructions for the Late Devonian through Triassic, PALEOMAP Progress Report 58-1193, Department of Geology, University of Texas at Arlington, Texas,10 p. 1993-31 Scotese, C.R., 1993. Phanerozoic Paleogeographic Maps, PALEOMAP Progress Report 40-1293, Department of Geology, University of Texas at Arlington, Texas, 29 p. (56h) 1993-32 Bocharova, N.Y. and Scotese, C.R., Revised Global Apparent Polar Wander Paths and Global Mean Poles, PALEOMAP Progress Report 56-1293, Department of Geology, University of Texas at Arlington, Texas, 20 p. (56n) 1993-33 Kraus, J.U., Walsh, D.B., and Scotese, C.R., 1993. Times of Global Plate Reorganization, PALEOMAP Progress Report 42-1293, Department of Geology, University of Texas at Arlington, Texas, 18 p. (56i) 1993-34 Bocahrova, N.Y., and Scotese, C.R., 1993. Plate Tectonic Evolution of the CIS, PALEOMAP Progress Report 57-1293, Department of Geology, University of Texas at Arlington, Texas, 26 p. (56o) 1993-35 Baumgardner, J., Bond, G., Coakley, B., Grotzinger, J., Gurnis, M., Hager, B., Kominz, M., Nummedal, D., O'Connell, R., Richards, M., And Scotese, C.R., 1993. Cooperative Studies of the Earth's Deep Interior (CSEDI): Plate Motions, Continental Geology and Sea Level Change, PALEOMAP Progress Report 49-1293, Department of Geology, University of Texas at Arlington, Texas, 26 p 1993-36 Bocharova, N.Y., Scotese, C.R., and Van der Voo, R., 1993. Global Apparent Polar Wander Paths in the Hotspot Reference Frame, PALEOMAP Progress Report 38-0193, Department of Geology, University of Texas at Arlington, Texas, 19 pp. lost hard copy? see 1993-32 1993-37 Kraus, J.U., Stephens, S., and Scotese, C.R., 1993. Catalog of Global Polygons and Plate Identification Numbers, PALEOMAP Progress Report 51-1293, Department of Geology, University of Texas at Arlington, Texas, 6 p. (56k) 1993-38 Kraus, J.U., and Scotese, C.R., 1993. PALEO-Refs Geologic Reference Database: A User's Guide, PALEOMAP Progress Report 54-1293, Department of Geology, University of Texas at Arlington, Texas, 23 p 1993-39 Scotese, C.R., 1993. Atlas of Plate Tectonic Reconstructions (0-800 Ma), PALEOMAP Progress Report 50-1293, Department of Geology, University of Texas at Arlington, Texas, 33 p dark copy , rescan 1993-40 Burkart, B., and Scotese, C.R., 1993. The Orizaba fault zone: missing link in the Neogene plate tectonic evolution of the southern Gulf of Mexico and Caribbean, American Geophysical Union, 1993 Fall Meeting, EOS, Transactions of the American Geophysical Union, v. 74, issue 43, p. 591. 1993-41 Jurdy, D. M., Stefanik, M., and Scotese, C.R., 1993. Paleozoic Plate Dynamics, American Geophysical Union, 1993 Fall Meeting, EOS, Transactions of the American Geophysical Union, v. 74, issue 43, p. 212. 1993-42 Walsh, D.B., and Scotese, C.R., 1993. Jurassic-Present Paleogeographic Evolution of the Marginal Bains of the South Atlantic, PALEOMAP Progress Report 46-1093, Department of Geology, University of Texas at Arlington, Texas, 14 p. 1993-43 Kraus, J.U., and Scotese, C.R., 1993. Global Polygons and Suture Map, PALEOMAP Progress Report 19-0293, Department of Geology, University of Texas at Arlington, Texas, 12 pp. (56c) something’s screwed up 1993-44 Bertrande, G., CRS Computer animation of SEAsia, ve4rsion 2a Quicktime 1994 1994-01 Scotese, C.R., 1994. Carboniferous paleocontinental reconstructions, in Cecil, C. Blaine, Edgar, N. Terence, Workshop on Predictive Stratigraphic Analysis; Concept and Application, U.S. Geological Survey, Reston, VA, United States. U.S. Geological Survey Bulletin, B2110, p. 3-6. (57b) 1994-02 Worsley, T. R., Moore, T. L., Fraticelli, C. M., and Scotese, C.R., 1994. Phanerozoic CO2 levels and global temperatures inferred from changing paleogeography, in Klein, George D., (editor), Pangea; paleoclimate, tectonics, and sedimentation during accretion, zenith and breakup of a supercontinent. Special Paper Geological Society of America, 288, p. 57-73, Boulder, CO. (58) Abstract: A simple model that tracks global land area and its average latitude to specify CO2 levels and consequent surface temperatures has been used to infer paleotem-peratures of 20 Phanerozoic global paleogeographic reconstructions. The model is based on the premise that global CO2 levels and temperature are directly proportional to the average latitude of the world landmass and inversely proportional to total land area. In all 20 cases, inferred CO2 and paleotemperature values are plausible and generally compatible with previous estimates. However, raw model output must be refined to take into account changes in rates of other climate modifiers such as orogeny, organic carbon burial, and precipitation that can be inferred from additional evidence. Results show a warm (19 degrees C) ice-free Cambrian world of small land area (75% emergent) at mid-latitudes (35 degrees ). Rapid equatorward migration of world landmass to 25 degrees latitude then led to a cool (13 degrees C) ice-capped late Ordovician world that was 70% emergent. Equally rapid migration back to higher latitudes (39 degrees ) by the Silurian coupled with decreased emergence (64%) produced the warmest temperatures of the Phanerozoic (22 degrees ). Return of the landmass to mid-latitudes (32 degrees ) coupled with reemergence (71%) by early Devonian reestablished cooler (18 degrees ) temperatures. As Pangea coalesced from early Devonian to late Carboniferous, percent emergence continually increased to virtually 100% as average latitude continually increased to 38 degrees , resulting in an ice-capped world of 16 degrees C. High organic carbon burial rates and orogeny at that time would suggest that our temperature estimates are slightly too high for this interval. By early Triassic, our results indicate continual iceenhanced emergence at virtually 100% and equatorward migration of land to 33 degrees latitude, yielding a global temperature of 16 degrees C. Other lines of evidence (absence of ice, low organic carbon burial, weak orogeny, aridity) suggest a slightly warmer world, or at least one with a lower pole-equator thermal gradient. From Triassic to mid Cretaceous, average latitude again increased to 38 degrees and emergence decreased to 75%, producing a warming of global temperature to 20 degrees C. Cretaceous to Recent results indicate that average latitude of the landmass decreases to 30 degrees as India and Australia move equatorward and that there is an increase to as much as 100% emergence during maximum late Cenozoic ice-sheet growth. Corresponding global temperatures decline to as low as 13 degrees C. 1994-03 Ross, M.I., Scotese, C.R., and Otto-Bliesner, 1994. Phanerozoic paleoclimatic simulations: A comparison of the parametric climate model and low resolution climate model, needs source 1994-04 Klein, G.D., Beauchamp, B., Baud, A., Chuvashov, B.I., Lopez-Gamundi, O.R., Parrish, J.T., Ross, C.A., Scholle, P.A., Scotese, C.R., and Watney, W.L., 1994. Introduction: Project Pangea and workshop recommendations, Geological Society of America Special Paper, v. 288, p.1-12. (59a) 1994-05 Bocharova, N. Yu., Pristavakina, E.I., and Zonenshain, L.P., 1993. Tectonic database and plate tectonic model of the former USSR Territory. Geological Society of America, Northeastern Section, 27th Annual Meeting, Abstracts with Programs, v. 25, Issue 1, p. 4. 1994-06 Walsh, D.B. and Scotese, C.R., 1994. Plate tracker version 1.1, User’s Guide, PALEOMAP Project, Department of Geology, University of Texas at Arlington, Texas. (59b) 1994-07 Golonka, J., Ross, M.I., and Scotese, C.R., 1994. Phanerozoic Paleogeographic and Paleoclimatic Modeling Maps, in A. F. Embry, B. Beauchamp, and D.J. Glass (editors), Pangea, Global Environments and rResources, Canadian Society of Petroleum Geologists, Memoir 17, p. 1-47. (57a) scan color versions 1994-08 Scotese, C.R., Walsh, D. B., and Bocharova, N.Yu., 1994. A Computer Animation of the Assembly of Asia, American Geophysical Union, 1994 Meeting, EOS, Transactions of the American Geophysical Union, v. 75, issue 16, p. 122. 1994-09 Scotese, C.R., Kraus, J. U., Bocharova, N.Yu., and Nie, Shangyou, 1994. Plate Tectonic Assembly of Asia: Comparision of Paleomagnetic and Paleoclimatic Constraints, American Geophysical Union, 1994 Meeting, EOS, Transactions of the American Geophysical Union, v. 75, issue 16, p. 126. 1994-10 Kraus, Jeffrey U., Walsh, David B., and Scotese, Christopher R., 1994. Timing, effects, and causes of reorganizations of the plate tectonic system, Annual Meeting Expanded Abstracts, American Association of Petroleum Geologists and Society of Economic Paleontologists and Mineralogists, v. 1994, p.190. 1994-11 Bocharova, Nataliya Yu., and Scotese, C.R., 1994. Plate tectonic reconstructions of the former Soviet Union from the Middle Devonian to the present, Geological Society of America, Northeastern Section, 27th Annual Meeting, Abstracts with Programs, v. 26, Issue 7, pp. 197-198. 1994-12 Maksimovic, Sladjana, and Scotese, Christopher R., 1994. Tectonic evolution of the Balkans, Geological Society of America, Northeastern Section, 27th Annual Meeting, Abstracts with Programs, v. 26, Issue 7, p.198. 1994-13 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 18. Miocene Lithologic Indicators of Climate, PALEOMAP Progress Report 80-0694, Department of Geology, University of Texas at Arlington, Texas, 20 p. 1994-14 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 17. Oligocene Lithologic Indicators of Climate, PALEOMAP Progress Report 79-0694, Department of Geology, University of Texas at Arlington, Texas, 13 p. 1994-15 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 16. Eocene Lithologic Indicators of Climate, PALEOMAP Progress Report 78-0694, Department of Geology, University of Texas at Arlington, Texas, 21 p. 1994-16 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 15. Paleocene Lithologic Indicators of Climate, PALEOMAP Progress Report 77-0694, Department of Geology, University of Texas at Arlington, Texas, 10 p. 1994-17 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 14. Late Cretaceous Lithologic Indicators of Climate, PALEOMAP Progress Report 76-0694, Department of Geology, University of Texas at Arlington, Texas, XX p. 1994-18 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 13. Lower Cretaceous Lithologic Indicators of Climate, PALEOMAP Progress Report 75-0694, Department of Geology, University of Texas at Arlington, Texas, 21. p. 1994-19 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 12. Upper Jurassic Lithologic Indicators of Climate, PALEOMAP Progress Report 74-0694, Department of Geology, University of Texas at Arlington, Texas, 11 p. 1994-20 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 11. Lower and Middle Jurassic Lithologic Indicators of Climate, PALEOMAP Progress Report 73-0694, Department of Geology, University of Texas at Arlington, Texas, 24 p. 1994-21 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 10. Later Triassic Lithologic Indicators of Climate, PALEOMAP Progress Report 72-0694, Department of Geology, University of Texas at Arlington, Texas, 20 p. 1994-22 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 9. Triassic Lithologic Indicators of Climate, PALEOMAP Progress Report 71-0694, Department of Geology, University of Texas at Arlington, Texas, 11 p. 1994-23 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 8. Middle and Upper Permian Lithologic Indicators of Climate, PALEOMAP Progress Report 70-0694, Department of Geology, University of Texas at Arlington, Texas, 17 p. 1994-24 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 7. Early Permian Lithologic Indicators of Climate, PALEOMAP Progress Report 69-0694, Department of Geology, University of Texas at Arlington, Texas, 14 p. 1994-25 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 6. Pennsylvanian Lithologic Indicators of Climate, PALEOMAP Progress Report 68-0694, Department of Geology, University of Texas atArlington, Texas, 33 p. 1994-26 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 5. Mississippian Lithologic Indicators of Climate, PALEOMAP Progress Report 67-0694, Department of Geology, University of Texas at Arlington, Texas, 18 p. 1994-27 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 4. Devonian Lithologic Indicators of Climate, PALEOMAP Progress Report 66-0694, Department of Geology, University of Texas at Arlington, Texas, 18 p. 1994-28 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 3. Silurian Lithologic Indicators of Climate, PALEOMAP Progress Report 65-0694, Department of Geology, University of Texas at Arlington, Texas, 6 p. 1994-29 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 2. Ordovician Lithologic Indicators of Climate, PALEOMAP Progress Report 64-0694, Department of Geology, University of Texas at Arlington, Texas, 15 p. 1994-30 Boucot, A.J., Chen Xu, and Scotese, C.R., 1994. Chapter 1. Cambrian Lithologic Indicators of Climate, PALEOMAP Progress Report 63-0694, Department of Geology, University of Texas at Arlington, Texas, 9 p. 1994-31 Ross, M.I., and Scotese, C.R., 1994. Computer-aided Plate Tectonic Modeling Course Notes, Geological Society of America Continuing Education Course #1, Saturday, October 22 and Sunday, October 23, 1994, Geological Society of America Annual Meeting, Seattle, WA, 48 pp. 1994-32 B. L. Otto-Bliesner, E. Becker, N. Becker, and Christopher Robert Scotese, 1994. Atlas of Phanerozoic Paleoclimate Simulated by a Global Climate Model, Center for Earth System History Technical Report No. 1, Center for Earth System History, Department of Geology, University of Texas, 149 pp. 1994-33 Bird, Robert T., Naar, David F., Scotese, C.R., and Larson, R.L., 1994. The kinematic history of the Juan Fernandez Microplate at the Pacific-Nazca-Antarctic triple junction, American Geophysical Union, 1994 Fall Meeting, EOS, Transactions of the American Geophysical Union, v. 75, issue 44, p. 609. 1994-34 Scotese, C.R., 1994. Late Ordovician and K/T Boundary paleogeographic maps, pp. 30 and 32, in Zimmer, C., Location, Location, Location, Discover, vol. 15, number 12, (December). 1994-35 Otto-Bliesner, B.L., and Scotese, C.R., 1994. The role of paleogeography in determining paleoclimate, in Palaeoclimates, Data, and Modelling (October, 1994), Gordon and Breach Publishers. 1994-36 Scotese, C.R., 1994. Research work mentioned in “Did the Earth ever freeze over?”, New Scientist, (july), vol. 143, no. 1936, p.17. 1995 1995-01 Jurdy, D. M., Stefanick, M., and Scotese, C.R., 1995. Paleozoic plate dynamics, Journal of Geophysical Research, v. 100, no. B9, pp. 17965-17975. (62) Abstract: Current plate motions can be accounted for by a balance of active forces, slab pull, ridge push, and, for continental plates, trench suction, with drag beneath the plate as a resistive force. If we assume that the same forces have acted through time, we can reconstruct plate motions from the geometry of past plate boundaries. Paleozoic reconstructions are made with paleomagnetic, tectonic, climatic, and biogeographic data, as no ocean floor remains. PALEOMAP reconstructions are used to estimate past plate speeds and to test simple dynamical models in order to determine which ranges of forces best accounts for the observations. Over the last 600 m.y., plate speeds averaged over 40- to 100-m.y. intervals show considerable variation; Gondwana's speed oscillates from 20 to 60 km/m.y. over a long timescale (200-400 m.y.) with considerable noise superposed. Over the Paleozoic Era motions for large continental regions average 28 km/m.y.; force balance models based on present-day observations suggest that continental regions without a large attached slab would move 30 mm/yr. The opening and closing of the ocean between Laurentia and Gondwana 560-400 Ma is used to test dynamical models and the parameter values assumed. In the late Precambrian, Laurentia rifted away from Gondwana. In the earliest Cambrian it was near 40 degrees S; by Late Cambrian and Ordovician it had moved to the equator. During the Silurian and Devonian, Laurentia reversed direction and later collided with Gondwana at 40 degrees S. In a model of the forces acting on the plates, slab pull, ridge push, and trench suction are assumed to balance plate drag. Only certain ranges of ridge-push and trench parameters can model both the opening and subsequent closing of the ocean. The dynamic models, with parameter values inferred from present rates, bracket the rates required by the reconstructions. 1995-02 Scotese, C.R. and Langford, R., 1995. Pangea and the Paleogeography of the Permian, in The Permian of Northern Pangea, P.A. Scholle, T. M. Peryt, and D. S. Ilmer-Scholle (editors), Volume 1, pp. 3-19, Springer-Verlag, Berlin. (63) 1995-03 Boucot, A. J., Chen, X. U., and Scotese, C.R., 1995. Ibexian and post-Ibexian paleogeography based on climatically sensitive sediments and biogeographic data, in Proceedings of the International Ordovican Symposium, Las Vegas, Nevada, June 12-16, pp. 291-295. (60) 1995-04 Golonka, J., and Scotese, C.R., 1995. Phanerozoic paleogeographic maps of Arctic margins, , in Proceedings of the International Conference on Arctic Margins (Magadan, Russia, September, 1994), K. Simakov and D. K. Thurston, ed., pp. 1-16. (61) 1995-05 Bird, R.T., Naar, D.F., Larson, R.L., and C.R. Scotese, New models for the origin and tecotonic development of the Juan Fernandez microplate, Programs and Abstracts, Canadian Geophysical Union, p. 49. 1995-06 Upchurch, G. R., Jr, Otto-Bliesner, B. L., and C.R. Scotese, 1995. Latest Cretaceous paleovegetation and global climate; comparison of proxy and model data, American Geophysical Union, 1995 Spring Meeting, EOS, Transactions of the American Geophysical Union, v. 76, issue 17, p. 182. 1995-07 Scotese, C.R., Otto-Bliesner, B. L., and Boucot, A., 1995. Comparison of the distribution of climatically sensitive sediments with vegetation habitat predictions made by paleoclimate modeling, American Geophysical Union, 1995 Spring Meeting, EOS,Transactions of the American Geophysical Union, v. 76, issue 17, p. 53. 1995-08 Scotese, C.R., 1995. Computer Animations Show Past and Future Continent Movements, Science News, A College of Science Publication, University of Texas at Arlington, Spring, 1995, p. 8. 1995-09 Otto-Bliesner, B.L., Boucot, A.J., and Scotese, C.R., 1995. New Earth System History Center Promotes Multidisciplinary Approach, Science News, A College of Science Publication, University of Texas at Arlington, Spring, 1995, p. 9. 1995-10 Scotese, C.R., in Foley, D.C., and T.Y. Ghazi, 1995. How Conoco uses GIS technology to map geology, geography through time, Oil & Gas Journal, May 8, 1995, vol. 93, no. 19, p. 74-77. 1995-11 Scotese, C.R., in Lessem, D., 1995. Land of the Giants, Earth, vol. 4, no. 4, p.32. 1996 1996-01 Golonka, J., Edrich, M. E., Ford, D. W., Pauken, R. J., Bochararova, N. Y., and Scotese, C.R., 1996. Jurassic Paleogeographic Maps of the World in The Continental Jurassic, M. Morales, ed., Museum of Northern Arizona Bulletin 60, p. 1-6. (66) no abs only figures 1996-02 Scotese, C.R., 1996. “Plate Tectonics”, in Encyclopedia of the Earth Sciences, Macmillan Publishing Company, New York, p. 859-864. (64) no abs have text 1996-03 Upchurch, G.R, Otto_Bliesner, B., and Scotese, C.R., 1996. Vegetation and warm climates during the Late Cretaceous, Sixth North American Paleontological convention, Special Publication - The Palaeontological Society, v. 8, p. 404. 1996-04 Scotese, C.R., 1996. “Paleogeography”, in Encyclopedia of the Earth Sciences, Macmillan Publishing Co., New York, p. 788-792. (65) no abs have text 1996-05 Seslavinky, K.B., Scotese, C.R., and Kusnetsov, N.B., 1996. The global Paleozoic paleogeography and paleotectonics of the continents, 30th International Geological Congress, Abstracts, v. 30-2, p.99. 1996-06 Scotese, C.R., 1996. Plate Tectonic & Paleogeographic Evolution of China, Short Course Notes prepared for the China National Oil & Gas Exploration & Development Corporation, Department of Geology, University of Texas at Arlington, TX, 99 pp. no abs have text 1997 1997-01 Boucot, A.J., Chen Xu, Scotese, C.R., Ruan Yiping, and Fan Junxuan, 1997. Correlation Between Geologically Marked Climate Changes and Extinction, (1997) Earth Science Frontiers, v. 4, no. 3-4, pp. 123-128. (70b) 1997-02 Boucot, A.J., Chen Xu, and Scotese, C.R., 1997. Correlation between geologically marked climate changes and extinctions, in Actualities paleontologiques en l’honneur de Claude Babin, Geobios, Memoire Special, 20, 55-59. (71) Abstract: The overall correlation between geologically widespread evidence for climatic zone boundary changes, and for major changes in the global climatic gradient, with extinction events is not strong. This may, of course, be partly a reflection of our poor understanding of past climates, as well as of past paleogeographies on which the climatic information is plotted. Still, at present the correlation in few cases can be easily interpreted as causal. The strongest cases can be made between the disappearance of cool to cold climates and the extinction of co-occurring cool to cold climate faunas, with the latest Ordovician Hirnantian Fauna, the mid-Middle Devonian Malvinokaffric Realm Fauna, and the bulk of the later Carboniferous-earlier Permian Gondwana Realm Fauna being good examples. 1997-03 Scotese, C. R., 1997. Early Paleozoic Plate Tectonic Reconstructions & Paleogeography, Program with abstracts, Geological Association of Canada & Mineralogical Association of Canada (GAC/MAC), Joint Annual Meeting, Ottawa, May 17-21, 1997, v. 22, p. 133. 1997-04 Ross, M.I., and Scotese, C.R., 1997. PALEOGIS: Using a Modern GIS to Create, Display, and Analyze Plate Tectonic and Paleogeographic Models, Program with abstracts, Geological Association of Canada & Mineralogical Association of Canada (GAC/MAC), Joint Annual Meeting, Ottawa, May 17-21, 1997, v. 22, p. 128. 1997-05 Scotese, C. R., 1997. Late Proterozoic Plate Tectonic Reconstructions & Paleogeography, Program with abstracts, Geological Association of Canada & Mineralogical Association of Canada (GAC/MAC), Joint Annual Meeting, Ottawa, May 17-21, 1997, v. 22, p. 133. 1997-06 Scotese, C.R., 1997. Mesozoic & Cenozoic Paleogeographic Atlas, PALEOMAP Project Progress Report 90-0497, PALEOMAP Prioject, Department of Geology, University of Texas at Arlington, TX, 52 pp. This Paleogeographic Atlas illustrates the plate tectonic development of the ocean basins and continents as well as the changing distribution of land and sea during the past 650 million years. The maps in this atlas are based on the paleogeographic maps of Scotese and Golonka (1992), but have been rendered in an artistic fashion to show the relief of mountain ranges and continental margins, active plate boundaries. The names of the ancient oceans and continents are shown (e.g. Panthalassic Ocean, Laurentia, Cimmeria) along with modern place names (in italic). The present-day coastlines, for reference, are overlain in light gray. Each paleogeographic map is a simplified black & white map showing only the ancient land areas and the present-day coastlines. The 20 time periods covered in this atlas are: 650 Ma (Late Proterozoic), 514 Ma (Late Cambrian), 458 Ma (Middle Ordovician), 425 Ma (Middle Silurian), 390 Ma (Early Devonian), 356 Ma (Early Carboniferous), 306 Ma (Late Carboniferous), 255 Ma (Late Permian), 237 Ma (Early Triassic), 195 Ma (Early Jurassic), 152 Ma (Late Jurassic), 94 Ma (Late Cretaceous), 69.5 Ma (latest Cretaceous), 50.2 Ma (Middle Eocene), 14.0 (Middle Miocene), 18,000 years ago (Pleistocene), Present-day, and three fanciful maps for 50, 150 and 250 million years in the future. A detailed description of the information used to make each map, the key features of each map, as well as some of the uncertainties associated with each map are described in the section that follows this introduction. 1997-07 Ross, M.I., Walsh, B. B., Eldridge, J. E., and Scotese, C.R., 1997. Computer Software to Produce Plate Tectonic Reconstructions, American Geophysical Union, Chapman Conference (abstract), June 17-22, Marshall, CA. Four different software packages have been developed that produce plate tectonic reconstructions: PGIS-Mac (Macintosh), Plate Tracker (PC), and Paleomapper (SunOS), and PALEOGIS (ArcView*). Three of these programs were written for specific hardware platforms (Mac, PC & Sun), the fourth application, PALEOGIS, because it uses an RPC (Remote Procedure Calls) architecture and runs under the ArcView 3.0* Geographic Information System (GIS), is largely platform independent. Though all four software packages produce plate tectonic reconstructions using the PALEOMAP Project plate model, their functionality varies. Plate Tracker (PC) produces plate reconstructions in 4 different map projections (Orthographic, Mercator, Mollweide, and Rectilinear). The user can specify a latitudinal and longitudinal map window, and output can be printed directly or saved as a Window's metafile. Both a DOS version and Windows 95 version of Plate Tracker are available. Paleomapper (SunOS) is an interactive plate modeling software package that works only on Sun platforms. Reconstructions and animations are produced using a dynamic orthographic map display. The user can manipulate a 3D globe in real-time and dynamically change the positions of the plates using scroll bars or "virtual" dials. This program requires supporting UNIX libraries, including PHIGS 3.0 and Motif. A similar program, developed for Silicon Graphics systems has been written by Dave Rowley, University of Chicago. Paleogeographic Information System for the Macintosh (PGIS-Mac) is the most versatile of the four plate reconstruction packages. PGIS-Mac produces plate reconstructions in 3 map projections (Mercator, Mollweide and Rectilinear) and runs best on Power PC versions of the Macintosh. The user can specify a latitudinal and longitudinal map window or center the map on any point on the globe. Plate reconstructions can be printed directly, saved in PICT format or saved as an ASCI text files that contain rotated map coordinates. Using an screen digitizing feature, the user can produce new map objects (points, lines, and polygons) that become a permanent part of the geographic data file. It is also possible to produce new plate reconstructions by dragging or spinning the continents. PGIS-Mac has limited GIS functionality. Associated with the geographic data are attribute tables which can be accessed and edited by the user. One of the most useful features of the program is the ability to produce QuickTime animations. PGIS-Mac replaces an earlier plate tectonic modeling program for the Macintosh, called Tern Mobilis. The PALEOGIS runs under ArcView 3.0* and is a true GIS. It is the most powerful of the four plate reconstruction packages because ArcView* handles all the visualization, cartographic, and database interaction. PALEOGIS produces plate reconstructions in more than a dozen map projections and runs best on PCs under Windows 95 or on UNIX workstations running SunOS. A Macintosh version, though largely untested, is also available. The user can specify the latitude and longitude of a map window or interactively center the map on any point on the globe. Plate reconstructions can be printed directly or saved in a variety of formats, including CGM, PostScript, and Adobe Illustrator. It is also possible to produce new plate reconstructions by dragging or spinning the continents. Because it is a GIS, ArcView has full SQL capabilities. Associated with the geographic data are attribute tables that can be searched and selected by the user. 1997-08 Scotese, C.R., 1997. In Search of a Meaningful Reference Frame: The best we can do, American Geophysical Union, Chapman Conference (abstract), June 17-22, Marshall, CA. The motion of the plates must be described relative to some point of reference outside the plate system. The hot spot reference frame and the paleomagnetic reference frame have both been used with some measure of success, though attempts to combine the two independent frames of reference have sometimes lead to confusing and contradictory results. Each reference frame has its strengths and weaknesses. The paleomagnetic reference frame has a well cataloged database of over 10,000 paleomagnetic determinations The number of the determinations is constantly increasing and the reliability continues to improve as more up-to-date techniques are used to verify the primary nature of the magnetic remanence. Paleomagnetic results are also available for every geological period, though there are considerably more paleomagnetic results for the Mesozoic and Cenozoic. On the other hand, paleomagnetic results vary in quality and reliability. This has often led to contradictory and confusing results (e.g. the controversy regarding the fit of the Atlantic-bordering continents; proposed plate velocities greater than 20 cm/yr). Because the paleomagnetic reference frame is the Earth's spin axis, there is a further limitation - only paleo-latitude can be estimated. The east-west position of the plates in unknowable from paleomagnetism. The Hot Spot reference frame has different set of strengths and weaknesses. If one agrees with the basic assumption of the hot spot reference frame, namely that there are "proper groups" of hot spots that are stationary with respect to each other, and with respect to the core mantle boundary, then the motion of the plates with respect to these fixed points can be precisely measured. The fact that there are a dozen or more active hot spots, produces a well-constrained solution with multiple, independent tests. The fact that hot spots often cross plate boundaries leads to further constraints. On the other hand, hot spot tracks on oceanic lithosphere only go back as far as the late Jurassic and in many cases it is often difficult to date the age of eruption along a hot spot track. Pre-Jurassic "continental" hot spot tracks have been suggested, but they are less reliable. The plate tectonic reconstructions produced as part of the PALEOMAP Plate Tectonic Atlas use a combined paleomagnetic and hot spot reference frame back to 130 million years ago. There is excellent agreement between the two reference frames. For this time interval, the global mean paleomagnetic pole, is on average less than 6 degrees from the location of the spin axis predicted by the hot spot reference frame. With the exception of hot spot results from the Pacific plate, there appears to be no systematic deviation through time, suggesting that True Polar Wander (TPW) during the Mesozoic and Cenozoic has been negligible. Though speculative, hot spot models using continental hot spots can be constructed back to the Devonian. These models often require rapid east-west shifts that are likely to be spurious. For this reason, prior to 130 million years ago, a purely paleomagnetic reference frame has been used. Rates of east-west motion are kept to a minimum and an attempt has been made to adhere to the principle of "minimum surprise". It should be noted that other techniques, such as: the timing of continental collision, the history of subduction, changing biogeographic affinities, latitudinal diversity gradients, and lithological indicators of climate, have also proven to be useful in constraining the relative positions of the continents. These techniques, have been used when appropriate, but do not provide sufficient contraints to form a reliable reference frame. 1997-09 Scotese, C. R., 1997. Plate Tectonic Reconstructions for the Last 1100 Million Years, American Geophysical Union Chapman Conference (abstract), June 17-22, Marshall, CA. An atlas and Geographic Information System (GIS) have been produced that illustrate the plate tectonic evolution of the Earth during the last 1100 million years. The maps and ArcView GIS show the location of active plate boundaries including: mid-ocean ridges, intracontinental rifts, subduction zones. Andean-type volcanism, fold & thrust belts, major strike-slip faults, and zones of continental collision. The maps and GIS also portray the past position of mid-ocean ridges (sea floor spreading isochrons) as well as major hot spot tracks and flood basalts. Educated guesses have been made concerning the configuration and evolution of plates, such as Panthalassic plate, Iapetan plate, and Paleo-Tethyan plate, that have been removed by subduction. The atlas and GIS consist of 50 maps. 8 maps show assembly and breakup of the supercontinents of Rodinia and Panotia during the Late Proterozoic (1100 - 545 Ma). 30 maps illustrate the assembly of Pangea during the Paleozoic and early Mesozoic and its subsequent breakup during the Jurassic and Cretaceous. The last 65 million years of plate tectonic evolution is shown by 12 plate tectonic reconstructions corresponding to major magnetic isochrons. Speculative maps portraying the evolution of the plates 50, 150 and 250 million years into the future have also been prepared. Documentation that accompanies the plate reconstructions includes: an index map describing the location and geographic extent of the plates, tectonic elements, and terranes that comprise the maps, tables of the euler poles used to reconstruct the relative position of the plates and tectonic elements, a summary and statistical analysis of the paleomagnetic poles used to orient the reconstructions relative to the spin axis, an indicator that describes the goodness of the fit between active hot spot locations and the hot spot tracks, a measurement of the congruence between the paleomagnetic and hot spot reference frames, and bibliography referring to the principal sources of information that were used to construct each map. *ArcView is a registereg trademark of ESRI 1997-10 Otto-Bliesner, B.L., and Upchurch, G.R., Jr., 1997. Vegetation induced warming of high-latitude regions during the Late Cretaceous period, Nature, vol. 385, number 27, p. 804-807. (70a) 1997-11 Scotese, C.R. Continental Drift Flip Book, 7th edition, PALEOMAP Project, Department of Geology, University of Texas at Arlington, Texas, 80 pp. (72) 1997-12 Arlington News 01/26/97 1997-13 Ross, M.I., and Scotese, C.R., 1997. QuickStart Guide to PaleoGIS for ArcView, Volume 1, Earth in Motion Technologies, Houston, TX, 45 pp. PaleoGIS is an ArcView extension and associated data sets that give a user the ability to create, display, and manipulate plate tectonic reconstructions. The PaleoGIS was created by Malcolm I. Ross (Earth in Motion Technologies) with help and inspiration from Stephen Gardoll (University of Western Australia). The default plate tectonic model that is provided with the PaleoGIS represents the of work of Dr. C. R. Scotese of the PALEOMAP Project at the University of Texas at Arlington. The PaleoGIS is sub-licensed from Earth in Motion Technologies by the PALEOMAP Foundation for distribution as part of the PALEOMAP Foundation Resource Pool. This document is intended to guide the user the user through the process of installing and running the PaleoGIS. It does not suppose to be a definitive reference for the software - rather it is styled as a cookbook, with step-by-step instructions to guide the user through the path required to achieve several common goals. The definitive reference - Reference Guide for the PaleoGIS by Malcolm I. Ross - is available from Earth in Motion Technologies as a separate document. 1997-14 Atlas of Earth History original negatives 1997-15 Paleogeographic Atlas Scotese & Golonka slides other #? 1998 1998-01 Upchurch, G.R., Otto-Bliesner, B.L., and Scotese, C.R., 1998. Vegetation-atmosphere interactions and their role in global warming during the latest Cretaceous, in Vegetation-climate-atmosphere interactions: past, present and future, D.J. Beerling, W.G. Chaloner, F.I. Woodward (editors), Phil. Trans. R. Soc. London, B. v. 353, issue 1365, p. 97-112. (77) Abstract: Forest vegetation has the ability to warm Recent climate by its effects on albedo and atmospheric water vapour, but the role of vegetation in warming climates of the geologic past is poorly understood. This study evaluates the role of forest vegetation in maintaining warm climates of the Late Cretaceous by (1) reconstructing global palaeovegetation for the latest Cretaceous (Maastrichtian); (2) modelling latest Cretaceous climate under unvegetated conditions and different distributions of palaeovegetation; and (3) comparing model output with a global database of palaeoclimatic indicators. Simulation of Maastrichtian climate with the land surface coded as bare soil produces high-latitude temperatures that are too cold to explain the documented palaeogeographic distribution of forest and woodland vegetation. In contrast, simulations that include forest vegetation at high latitudes show significantly warmer temperatures that are sufficient to explain the widespread geographic distribution of high-latitude deciduous forests. These warmer temperatures result from decreased albedo and feedbacks between the land surface and adjacent oceans. Prescribing a realistic distribution of palaeovegetation in model simulations produces the best agreement between simulated climate and the geologic record of palaeoclimatic indicators. Positive feedbacks between high-latitude forests, the atmosphere, and ocean contributed significantly to high-latitude warming during the latest Cretaceous, and imply that high-latitude forest vegetation was an important source of polar warmth during other warm periods of geologic history. 1998-02 Scotese, C.R., 1998. Animation: Continental Drift, 0-750 million years (paleogeography.mov, Quicktime format), PALEOMAP Project, www.scotese.com, Evanston, IL. 1998-03 Scotese, C.R., 1998. What we really don’t know about the plate tectonic, palaeogeographic, palaeoclimatic and biogeographic history of Gondwana in J. Almond et al., (editors), Special Abstracts Issue, Gondwana 10: Event Stratigraphy of Gondwana, Journal of African Earth Sciences, v. 27, n. 1A, p. 173-174. During the past 20 years, as a result of careful revisions and refinements, the broad plate tectonic, palaeogeographic, palaeoclimatic, and biogeographic history of Gondwana has become well known. The supercontinent of Gondwana was wrought during the Pan-African collisional event (600 Ma ago) and remained intact for over 400 Ma. During that time interval it crossed the South Pole, joined the northern continents to form Pangaea, and split apart in 3 distinct phases beginning in the Early Jurassic and ending in the Late Cretaceous. So what else is new? What more is there to know? Lots. Though the broad outline is well known, important questions remain unanswered. Regarding its formation, 'How many continents were involved?', 'What was the exact timing of collision between these pieces?', 'What was the polarity of subduction?', 'When, exactly, was the process finished?'. 'What, if anything, did the formation of Gondwana have to do with the Vendian Ice Age, or the diversification of metazoans?'. Gondwana was largely intact, and traversed the South Pole during the Palaeozoic, however, the details of its Palaeozoic history are not well known. For instance, 'What initiated subduction along the Tasman-Transantarctic-Cape Trend?'. 'Does palaeomagnetic and palaeoclimatic eyidence from Gondwana support a period of rapid True Polar Wander during the Late Precambrian-Early Cambrian?', 'What path did Gondwana take as it crossed the South Pole? Was it slow, steady, or rapid with loops and twirls?'. 'How extensive was the Late Ordovician Ice sheet?, Did it really stretch from Cape Town to Yemen?', and 'Can we make sense out of the history of terrane accretion in southern South America and eastern Ausutralia?'. During the Early Palaeozoic, the Cathaysian and Cimmerian Terranes seemed to be associated with the Indo-Australian region of Gondwana, 'Where exactly were they located?', and 'When did they rift away from Gondwana?'. Biogeographically speaking, 'What does the distribution of the earliest fossil fish tell us about Siluro-Devonian palaeogeography?', 'When did the first terrestrial vertebrates arrive in Australia?', and 'Where did they come from?'. The Early Jurassic through Late Cretaceous break-up of Gondwana is well documented by geological, tectonic, and marine geophysical data, however a few nagging questions remain. 'Are the Karoo rifts a precursor to Gondwana break-up, or an earlier, unrelated event?', 'What was the fit of the continents that comprised eastern Gondwana?', 'Was it a loose fit or a tight fit?', 'How exactly does India fit against Madagascar?', 'What went in that gap between northwestern India and Arabia?', 'What rifted away from northwestern Australia?', 'Was there a large chunk of continental crust north of India (Greater India)?', 'Where did it go?'. Concerning the break-up of Gondwana: 'Were the Early Jurassic flood basalts of South America, South Africa, and East Antarctica produced by a hot spot, or do they signal the beginning of break-up?', 'Why did Gondwana break apart, in the first place?', 'Why did the break-up take place in 3 distinct stages {Middle Jurassic, Early Cretaceous. Late Cretaceous)?'. During the Late Cretaceous. Gondwona was in its final phase of dispersal, yet important questions remain, 'Why can't we get the older M anomalies to fit togther properly?', 'What caused the Deccan flood basalts?', 'Is there a relationship between these flood basalts and the K/T extinction?', 'When was the ligation between Africa and South America terminated?', and 'How did those darn dinosaurs get from Africa to India in the Late Cretaceous?!'. I would like answers to these questions. Realizing, however, that it is often easier to ask questions rather than seek out solutions, I would like to review various solutions and relate my own answers to these questions, however fantastic and controversial they may be. 1998-04 Boucot, A.J., Ross, M.I., and Scotese, C.R., 1998. Jurassic plate tectonic, paleogeographic, and paleoclimatic reconstructions. Abstracts and Programs, 5th International Symposium on the Jurassic, IUGS, Episodes, v. X, pp. 83-84. 1998-05 Scotese, C.R., 1998. Gondwana’s climate changes, in J. Almond et al., (editors), Special Abstracts Issue, Gondwana 10: Event Stratigraphy of Gondwana, Journal of African Earth Sciences, v. 27, n. 1A, p. 172-173. Climate can change on two scales: globally and regionally. Regional climatic change is simply the result of movement of a continent across Earth's climatic zones. During its long history Gondwana crossed numerous climatic belts. During the Late Precambrian and Early Palaeozoic this was especially true for the western part of Gondwana (northern South America and western Africa), which moved from south polar latitudes to equatorial latitudes. In contrast, Australia. Antarctica and the Cathaysian Terranes of northeastern Gondwana remained at relatively low latitudes throughout most of the Early and Middle Palaeozoic. The opposite was true for the Late Palaeozoic and Early Mesozoic. Eastern Gondwana (India and Australia) moved rapidly from subtropical to polar latitudes during the Carboniferous, Permian and Triassic, while the western half of Gondwana (northern South America and western Africa, remained at subtropical latitudes. During the Jurassic and Cretaceous the general tendency has been for all the Gondwana continents to move northward, either from subtropical to equatorial positions (Africa, Arabia, and India), or from temperate to tropical positions (Australia). Antarctica has remained near the South Pole for 300 Ma and South America, though it has shifted westwards, has not changed latitude by more than 20 degrees during the last 300 Ma. Superimposed on regional climate change is a global climatic signal.. During the 400 Ma that Gondwana existed, the Earth's global climate system shifted from 'Ice House' conditions to ’Hot House' conditions four times (Fig. 1). The first Ice House episode was the great Vendian Ice Age, which was just ending as Gondwana became fully assembled. The collisions which formed Gondwana may have a had a role in creating Ice House conditions during the Late Precambrian. This Ice House world was followed by global warming during the Cambrian and Early-Middle Ordovician. The second Ice House episode was a brief, but extensive period of global cooling during the latest Ordovican ( earliest Silurian?). It was followed by global warming from the Silurian through to the Middle Devonian. The third episode of Ice House conditions began in the Late Devonian-Early Carboniferous, expanded during the Middle Carboniferous (Namurian B), and terminated during the Early Permian (Artinskian). This Ice House world was followed by global warming during the Late Permian, Triassic, and Early and Middle Jurassic. Geological indicators of climate and palaeontological evidence suggests that Earth may have experienced 'run away' greenhouse warming at the end of the Palaeozoic. This 'Super Hot House World' may have been responsible for the Late Permian mass extinction event. The final episode of global cooling, during the Late Jurassic and Early Cretaceous, was a 'mild' Ice House episode, by all accounts. It was followed by the Cretaceous and Early Tertiary Hot House World. In this presentation, palaeoclimatic reconstructions will be presented for 8 time intervals, corresponding to the 4 major Ice House (I) and Hot House (H) couplets: (I1) Vendian (650 Ma), (H1) Late Cambrian Early Ordovician (500 Ma); (I2) Late Ordovician (450 Ma), (H2) Siluro- Devonian (400 Ma); (I3) Late Carboniferous-Early Permian (300 Ma), (H3) Early Triassic (240 Ma); and (i4) Late Jurassic-Early Cretaceous (140 Ma), (H4) Late Cretaceous (80 Ma). The changing distribution of climatically sensitive lithofacies, such as coals, evaporites. calcretes, bauxites, kaolinites. glendonites and tillites, will be plotted on maps, as well as the results of recent palaeoclimatic simulations. 1998-06 Bird, T. R., Naar, D. F., Larson, R. L., Searle, R. C., and Scotese, C.R., 1998. Plate reconstruction of the Juan Fernandez Microplate: Transformation from internal shear to rigid rotation, Journal of Geophysical Research, v. 103, issue B4, p. 7049-7067. (73) Abstract: Side-scan sonar, swath bathymetry and magnetic anomaly date define a detailed, three-phase history of the Juan Fernandez microplate. The approximately 6 m.y. history is presented in a series of discrete time steps to document the growth and reorganization of propagating spreading centers and structural feature, and microplate kinematic evolution. Prior to the microplate, the East Pacific Rise at the Pacific-Antarctic-Nazca triple junction was offset by a long transform fault zone, likely the fastest slipping transform on Earth at anomaly 3A time. The microplate originated from an intratransform setting between anomaly 3A (5.95 Ma) and anomaly 3 (5.24 Ma) time. Its early development resembled a large propagating rift system, and microplate core structures suggest the entire offset zone may have experienced deformation. Fast propagation of the East Ridge dominated microplate growth until approximately 2.6-1.9 Ma when seafloor spreading became the dominant growth process. The microplate rotation rate increased threefold (from 9 to 29 degrees m.y. (super -1) average) from phase 1 (4.2-2.6 Ma) to phase 2 (2.6-1.1 Ma) of the microplate's history, then reduced fourfold (29 to 7 degrees m.y. (super -1) average; phase 3, 1.1 Ma to Present). Phases 2 and 3 of the microplate's rotational history support the edge-driven model for microplate kinematics of Schouten and others to a good approximation. The Pacific-Nazca shear couple drove microplate rotation during phase 2, but development of the southeastern boundary enabled a transfer to the Nazca-Antarctic plate pair (phase 3). West Ridge propagation and reorganization of the south-western boundary may have decoupled the Pacific plate from the microplate, thus facilitating the shear couple transfer. The recent continued deceleration in microplate rotation rate and westward migration of the Pacific-Antarctic ridge axis relative to the microplate may indicate that the process of microplate "death" has begun. We speculate that the Juan Fernandez microplate will accrete to the Antarctic plate, perhaps within the next million years, like the extinct Friday microplate has done, thereby accomplishing another northward migration of the Pacific-Antarctic-Nazca triple junction. Our reconstructions illustrate that the Easter and Juan Fernandez microplates are more similar than previously thought in terms of their origin, growth, rift propagation, ridge segmentation and overall tectonic evolution. 1998-07 Scotese, C.R., 1998. Animation: Lithologic Indicators of Paleoclimate (Paleocliamte.mov, Quicktime format), PALEOMAP Project, www.scotese.com, Evanston, IL. 1998-08 Scotese, C.R., 1998. Animation: Future Plate Motions, (Future+250Ma.mov, Quicktime format), PALEOMAP Project, www.scotese.com, Evanston, IL. 1998-09 Scotese, C.R., 1998. Animation: Rodinia to Pacific, (Rodinia_Pacific.mov Quicktime format), PALEOMAP Project, www.scotese.com, Evanston, IL. 1998-10 Scotese, C.R., 1998. Animation: Seafloor Spreading and LIPS, (sfs.mov, Quicktime format), PALEOMAP Project, www.scotese.com, Evanston, IL. add to bibllio 1998-10b 0-750Ma .mov 1998-11 Scotese, C.R., 1998. Computer software to produce plate tectonic reconstructions, in J. Almond et al. (editors), Special Abstracts Issue, Gondwana 10: Event Stratigraphy of Gondwana, Journal of African Earth Sciences, v. 27, n. 1A, pp. 171-172. Four different software packages have been developed to produce plate tectonic reconstructions: Plate Tracker for Windows, Palaeocontinental Map Editor (PCMEJ for Windows/NT, Palaeogeographic Information System for the Macintosh (PGIS/Mac), and PalaeoGIS for ArcVicw (by ESRI). Though all four software packages produce plate tectonic reconstructions based on the PALEOMAP Project global plate tectonic model, their user-friendliness and functionality varies considerably. Plate Tracker, co-authored with David B. Walsh and John Eldridge, produces plate tectonic reconstructions for any time interval back to 750 million years, in 4 different map projections (Orthographic, Mercator, Mollweide and Rectilinear). It was written in Visual Basic and has an intuitive graphical user interface. The user can specify a latitudinal and longitudinal map window and output can be printed directly or saved as a Windows bit-mapped image. PCME, co-authored with Antonio Schettino, is a highly interactive program that presents the changing configuration of land and ocean in a series of 30 rotatable globes. Using buttons and scroll bars the user can rotate the globes in real-time to view and centre on areas of special interest. The palaeogeographic globes are rendered with coloured, shaded polygons that show the past locations of mountain belts, land areas, shallow seas and deep ocean basins. A present-day coastline can be overlain on the globes to show the location of familiar geographic features. Static maps in several other map projections can also be plotted. PGIS/Mac, co-authored with Malcolm I. Ross, is a multifunctional program that allows users to plot plate reconstructions and palaeogeographic maps in 3 different map projections (Mollweide, Rectilinear and Mercator). Point, line and polygon formats are all supported. The user can easily import user-defined point data (ASCI, tab delimited format) that will automatically plot in reconstructed coordinates. It is also possible to digitise on the screen using the mouse. The digitised point, line or polygon data will reconstruct with the continents if a new time interval is chosen. The maps can be saved in PICT format or as QuickTime animations. PGIS/Mac also allows the user to interactively move and reposition the continents. The PalaeoGIS, co-authored with Malcolm I. Ross, runs under ArcView (an ESRI product) and is a true, full-featured GIS. It is the most powerful of the four programs because ArcView handles all the visualisation, cartographic transformations, and SQL database queries. PalaeoGIS produces plate reconstructions in more than a dozen map projections. The user can specify the map scale and centre the projection on any point on the globe. Plate tectonic and palaeogeographic reconstructions can be printed directly or saved in a variety of formats, including CGM, BMP, WMF, EPS and Adobe Illustrator. It is also possible to produce new plate tectonic reconstructions by dragging or spinning the continents about user-defined poles of rotation. Associated with the geographic data are attribute tables that can be searched and selected by the user. The PalaeoGIS requires an installed version of Arcview, version 3.0 or later. 1998-12 Scotese, C.R., 1998. A tale of two supercontinents: the assembly of Rodinia, its break-up, and the formation of Pannotia during the Pan-African event, in J. Almond et al. (editors), Special Abstracts Issue, Gondwana 10: Event Stratigraphy of Gondwana, Journal of African Earth Sciences, v. 27, n. 1A, pp. 171. Recent tectonic syntheses by I. Dalziel. P. Hoffman, E- Moores, and J. Rodgers, as well as palaeomagnetic summaries by J. Meert, C. Powell, T. Torsvik, and R. van der Voo, have led to the proposal that there were two Late Precambrian supercontinents: Rodinia and Pannotia. Rodinia formed during the Grenville event 1-1100 Ma) and broke apart approximately 750 Ma ago. The rifted fragments of Rodinia sequentially collided during the Pan- African Orogeny (700-550 Ma) forming a new supercontinent, Pannotia. Though the exact Size end configuration of Rodinia is not known, it appears that North America formed the core of this supercontinent. The cast coast of North America was adjacent to western South America and the west coast of North America lay next to Australia and Antarctica. About 750 Ma ago, Rodinia collided with a smaller continent, the Congo Craton. This collision is marked by the Mozambique Granulite Belt of East Africa. As shown in Fig. 1, this collision may have triggered the break-up of Rodinia. Rodinia split into two halves, opening the Panthalassic Ocean. North America, together with Baltica. Siberia, and the Saharan and Amazonian Cratons, rotated southward towards the South Pole. The other half of Rodinia. composed primarily of East Gondwana {Antarctica. Australia, India. Arabia) and the continental fragments that would one day become China and the Middle East, rotated counter-clockwise, northwards across the North Pole. Between the two halves of Rodinia lay a third continent, the Congo Craton, made up of much of north central Africa. From 750 to 600 Ma, the Mozambique Seaway between the northern half of Rodinia (East Gondwana) and the Congo Craton progressively closed. Oceanic crust was subducted beneath the Congo Craton. generating the Hijaz island-arc of Cgypt, Arabia and Sudan. On the south side of the Congo Craton, the Pan-African Ocean was consumed as the southern half of Rodinia {the Saharan and Amazonian Cratons, among others), swung northward, eventually colliding with the Congo Craton between 650 and 550 Ma (Fig. 1). The sequence of continental collisions that started 750 Ma ago and continued to the end of the Precambnan {approximately 550 Ma) assembled the supercontinent of Pannotia, with Gondwana at its core. Pan-African mountain building produced a series of mountain ranges of Himalyan proportions. These mountain ranges occupied low palaeolatitudes and, like the modem Himalayas, may have triggered the episode of Vendlan glaciation. The supercontinent of Pannotia was short lived and began to rift apart in the latest Precambrian (-570 Ma). Plate tectonic reconstructions for 1100, 850, 750, 700. 650, 600 and 550 Ma. together with a computer animation of plate motions during the same time interval will be shown. A palaeogeographic reconstruction showing the ancient distribution of mountains, land, shallow sea, and deep sea will be presented for 650 Ma (Vendian Ice Age). It is suggested that the Vendian Ice Age was mainly due to palaeogeographic effects, namely the location of land areas near the poles, and the presence of Himalyan-sized mountain ranges near the Equator. 1998-13 Kazmin, V.G., Natapov, L.M., Bush, W.A., Filipova, I.B., Jasamanov, N.A., Balukhovsky, A.N., Volkov, J.V. Gatinsky, J., Kalimulin, S.M., Kulikova, L.I., Miledin, A.K., Pugacheva, I.P., Suetenko, O.D., Bocharova, N.J., Zonenshain, L.P., Kononov, M.K., and C.R. Scotese, 1998. The Paleogeographic Atlas of Northern Eurasia, Institute of Tectonics of Lithospheric Plates, Institute of Lithospheric Plates, Moscow, Russia, (26 maps). (76) 1998-14 Scotese, C.R., Ross, M.I., and Schettino, A., 1998. Plate Tectonic Reconstructions and Animations, American Geophysical Union 1998 Spring Meeting, EOS, Transactions of the American Geophysical Union, v. 79, issue 17, p. 334. 1998-15 Scotese, C.R., Bryant, N., Burchfiel, B.C., Buber, B.T., Siever, R., and Zachos, J., 1998. Millennium in Maps, Physical Earth, Earth in Flux, National Geographic Magazine, v. 192, no. 5, May 1998 (map supplement featuring paleogeographic maps). rescan color maps (74) 1998-16 Russell, D.A., Wheeler, E.A., and Scotese, C.R., 1998. Dinosaurian environments of the Saharan Cretaceous, DINOFEST, Philadelphia, PA, June, 1998. 1998-17 Chatterjee, S., and Scotese, C.R., 1998. Dinosaurs in the Land of the Gonds, Society of Vertebrate Paleontologists, 58th Annual Meeting, Snowbird, Utah, September 30-October, 3, 1998, (abstract), Journal of Vertebrate Paleontology, v. 18, issue 3, supplement, p. 33 1998-18 Walsh, D. B., Kraus, J.U., Barnes, K.R., and Scotese, C.R., 1998. Plate Tectonic Modeling and Tectono-Stratigraphic Evolution of the South Atlantic Borderlands: An integrated Paleogeographic synthesis, American Association of Petroleum Geologists International Conference and Exhibition, Buenos Aires, November 1998, AAPG Bulletin, v. 82, issue 10, p. 1980. Abstract: This study was initiated to examine the cause and effect relationships of regional plate tectonic processes upon the tectono-stratigraphic evolution of the South Atlantic marginal basins. Evidence from twenty basins along the South American and African margins suggests that temporal and spatial variations in plate kinematics and intraplate stress regimes profoundly affect basin evolution. Perturbations in plate motions are commonly recorded by unconformities or periods of rapid subsidence along extensional margins. Two fundamental controls on the plate tectonic to basin evolution relationship are the location of basins to preexisting crustal weakness and the diachronous nature of the opening. Evidence from gravity and surface maps indicate that rift basins preferentially formed along the north-northeast trending basement structural fabric formed during the Neoproterozoic Braziliano-Pan African orogeny (700-500 Ma). Likewise, basin stratigraphic evolution (pre-rift, rift, drift packages) correlates well with the south to north progression of ocean opening. A series of ten paleogeographic maps and stratigraphic columns illustrate the Late Jurassic to present-day plate tectonic and tectono-stratigraphic evolution of the South Atlantic borderlands. 1998-19 Jenkins, G. and Scotese, C.R., 1998. An early Snowball Earth?, Science, v. 282, pp. 1644-1646. (75) 1998-20 Scotese, C.R., 1998. A Look at Earth History Through Maps, The Neatline, A Newsletter of the Texas Map Society, vol. 1, number 3, p. 5. 1998-21 Scotese, C.R., 1998. Millennium in Maps, Physical Earth, Map Supplement, National Geographic, vol. 192, no. 5, May, 1998. 1998-22 Mapping the Earth UIC Alumni Mag 1998-23 Arlington Morning News 1998-24 Scotese, C.R., 1998. Paleogeographic Atlas, in Natural Section, Natural History Magazine, volume 107, number 3, April, 1998, pp.6-7. 1998-25 Map from Animation & Narration see 1998.02 1999 1999-01 Upchurch, G.R., Otto-Bliesner, B.L., and Scotese, C.R., 1999. Terrestrial vegetation and its effects on climate during the latest Cretaceous, E. Berrera and C. Johnson, (eds), the Evolution of Cretaceous Ocean/Climate systems, Geological Society of america Special Paper, v. 332, pp. 407-426. XXXX (reduce and add to RG, add color figures) (79) needs abs? 1999-02 Chatterjee, S. and Scotese, C.R., 1999. The Breakup of Gondwana and the Evolution and Biogeography of the Indian Plate, in Gondwana Assembly: New Issues and Perspectives, Ashok Sahni and R.S. Loyal (editors), Proceedings of the Indian National Science Academy, Part A: Physical Sciences, v. 65A, No. 3, pp. 397-425. (80) Abstract: The palaeopositions of India after its breakup from Gondwana and its subsequent northward journey during the Mesozoic and Early Palaeogene pose many plate tectonic and palaeobiogeographic riddles. Most reconstructions show peninsular India separating from Gondwana, and remaining an island continent for more than 100 million years until it collided with Asia. However, the lack of endemism among Indian Cretaceous terrestrial vertebrates is clearly inconsistent with the island continent hypothesis. A new model for the tectonic evolution of the Indian plate from its Pangean origin to the present day is proposed that is well constrained by geological and geophysical evidence. In this model, a previously unrecognized land area, called Greater Somalia, occupied the position between eastern Arabia and northwestern India. During the Late Jurassic, India rifted away from Greater Somalia. Throughout most of the Cretaceous India was separated from the rest of Gondwana but in the latest Cretaceous it reestablished contact with Africa through Greater Somalia. India maintained contact until the Eocene Period when it collided with Asia. Based on this plate tectonic model, 14 new paleogeographic maps are presented showing the evolution of the Indian plate from its Pangean origin to its final union with Asia. An area cladogram identifies the 11 nodes of hierarchial tectonic evolution of the Indian plate during the last 250 million years. A major question of Indian palaeobiogeography is how the terrestrial vertebrates such as dinosaurs responded to fragmentation of India from Gondwana. The similarities and differences between Indian vertebrates with those of other continental fragments provide an independent check for a number of key events during its tectonic evolution. Using the plate tectonic reconstructions as a guide, the distributions of dinosaurs and other vertebrates during the Mesozoic and Early Cenozoic are discussed. A close correspondence between the continental position of India and the distribution of vertebrates is generally observed. However, the Indian vertebrate fauna seems more closely related to Europe at the familial level to that of Africa during the Mesozoic. This disjunct endemism of fossil distribution pattern may reflect poor sampling from the intervening Africa. Whenever Indian vertebrate records are missing from certain geologic periods, their compositions are inferred from the contemporary animals in adajacent landmasses. The Late Triassic and Jurassic vertebrates of India are cosmopolitan in the Pangean world indicating various transcontinental migration routes. Four such dispersal routes are identified, northern, central, southern and western. During the mid-Cretaceous, India became isolated and these dispersal routes were closed. During the Late Cretaceous (approximately 70 Ma), the northern route across the Greater Somalia was reopened allowing immigration of dinosaurs and other vertebrates from Africa and Europe. This northern dispersal route explains for the first time why the Indian Maastrichtian vertebrates do not show any evidence of endemism. About 65 million years ago, the Shiva impact event at the Indo-Seychelles boundary and the Chicxulub impact in Mexico triggered a biotic catastrophe and led to the demise of dinosaurs and other organisms. Mammals rebounded from this catastrophe and became the dominant land vertebrates during the early Tertiary. Fossil evidence suggests that India made the initial contact with Asia during the Eocene and opened a new northeastern corridor for faunal interchange. 1999-03 Scotese, C.R., Boucot, A.J., and McKerrow, W.S., 1999. Gondwanan paleogeography and paleoclimatology, in Gondwana 10: Event Stratigraphy, Journal of African Earth Sciences, v. 28, issue 1, pp. 99-114. (78) 1999-04a Hecht, J., and Scotese, C.R., 1999. The Ages of Earth: A Four Billion Year Atlas of Our Planet, (March, 1999), ISBN 0-02-550171-2. 1999-04 Bice, K. L., and Scotese, C.R., A reexamination of the role of Geography and Poleward Heat Transport in the Cenozoic Global Cooling Trend, American Geophysical Union 1999 Spring Meeting, EOS, Transactions of the American Geophysical Union, v. XX, issue XX, p. XXX. 1999-05 Scotese, C.R., Devonian Paleogeographic Reconstructions, p. 117, in Westenberg, K., 1999. The Rise of Life on Earth: From Fins to Feet, National Geographic Magazine, (May, 1999), vol. 195, no. 5, National Geographic Society, Washington, D.C. 1999-06 Scotese, C.R., Nokleberg, W.J., Scholl, D.W., Bundtzen, T.K., Khanchuk, A.I., Monger, J.W.H., Dawson, K.M., Norton, I.O., and Parfenov, L.M., 1999. Metallogenic and Tectonic Development of the Circum-North Pacific: A Computer Animation, Geological Society of America Cordilleran section Centennial 1899-1999, June 2-4, 1999, Berkeley, CA, Abstract with Programs, v31, no. 6, p. 93. add animation 1999-07 Scotese, C.R., 1999. Breaking Plates, in Netwatch:Cool Images, Jocelyn Kaiser (editor), Science, June 18, 1999, volume 284, p. 1887. 1999-08 Scotese, C.R., 1999. Late Cretaceous Plate Reconstructions - Constraints and Problems, in Terrane Accretion along the Western Cordilleran Margin: Constraints on Timing and Displacement, (abstract), Penrose Conference, Winthrop Washington, June 21-27, 1999. 1999-09 Boucot, A.J., Xu, Chen, and Scotese, C.R., 1999. Phanerozoic climate distribution and paleogeography, in UNESCO-IGCP Project 421, North Gondwanan mid- Paleozoic bioevent/biogeography patterns in relation to crustal dynamics, Abstract book, Peshawar Meeting IGCP 421, 8-26 September, 1999, p. 41-42. 1999-10 Scotese, C.R., 1999. Teaching Earth System History: A Computer Assisted Approach, Geological Society of America Short Course Notes, Geological Society of America Annual Meeting, October 24, 1999, Denver, CO, 171 pp. 1999-11 Scotese, C.R., 1999. The History of the Earth and its Continents as Seen Through Computer Animation, Friends of the UTA Libraries, November 5, 1999, UTA Central Library, University of Texas at Arlington, TX. 2000 2000-01 Bice, K., Scotese, C.R., Seidov, D., and Barron, E.J., 2000. Quantifying the role of geographic change in Cenozoic ocean heat transport using uncoupled atmosphere and ocean models, Palaeogeography, Palaeoclimatology, and Palaeoecology, v 161, pp. 295-310. (81) Abstract: A series of five Cenozoic atmospheric general circulation model (AGCM) experiments has been performed using a new set of paleogeographic reconstructions for 55, 40, 33, 20 and 14 Ma. The five continental reconstructions incorporate the tectonic evolution of early Eocene to middle Miocene continental positions and topography. With all other model boundary conditions and forcings held constant, the series of AGCM experiments captures a <1 degrees C decrease in annual mean temperature through the Paleogene and early Neogene. Regional and seasonal differences among the five experiments are small in magnitude, but are consistent with the imposed paleogeographic changes. From the AGCM experiments alone, it might be concluded that changes in continental positions had little impact on Cenozoic climate change. However, ocean configuration changes between 55 and 14 Ma, especially gateway openings and closures, are expected to produce significant changes in ocean thermohaline circulation, a system that cannot be simulated by the slab ocean model component of an AGCM. The nature of changes in ocean heat transport and thermohaline circulation arising from the evolution of early Eocene through middle Miocene ocean basin configurations is examined in a series of five global, three-dimensional ocean model experiments forced by output from the AGCM. The ocean model suggests that paleogeographic change throughout the Cenozoic has caused changes in the interhemispheric partitioning of heat transport and that the modern shape of the ocean heat transport curve has evolved in response to ocean basin evolution. The prediction of very low ocean heat transport in the Northern Hemisphere of the early and middle Eocene suggests a much more important role for atmospheric heat transport in the temperate polar climates of the Eocene than is generally acknowledged. Results suggest that Southern Hemisphere ocean heat transport decreased throughout the interval 55-14 Ma. The results also show that, in the absence of reliable coupled models for paleoclimate studies, full three-dimensional ocean models must be used in parallel with slab ocean AGCMs if we wish to understand the true effects of paleogeographic change on climate and the true nature of past ocean heat transport. 2000-02 Scotese, C.R., 2000. “Laurasia”, article for print and electronic versions of Encyclopedia Britannica. (85) 2000-03 Scotese, C.R., 2000. “Paleogeography”, article for print and electronic versions of Encyclopedia Britannica. (83) find color EB maps 2000-04 Nokleberg,W.J., Scotese, C.R., Khanchuk, A.I., Monger, J.W.H., Dawson, K.M., Norton, I.O., Parfenov, L.M., and Stone, D.B., 2000. Dynamic computer model for the Phanerozoic tectonic and metallogenic evolution of the Circum-North Pacific, Geological Society of America, Cordilleran Section and associated societies, 96th annual meeting, Abstracts with Programs, v. 32, issue 6, p. 59-60. Abstract: A dynamic computer model, based on a geologic and tectonic analysis of the region, illustrates the complex Phanerozoic tectonic evolution of the Circum-North Pacific. The model, produced by computer morphing of a series of fourteen paleogeographic maps, illustrates the major tectonic and metallogenic events for seven major time intervals. (1) In the Late Proterozoic, and Late Devonian and Early Carboniferous, major periods of rifting, as well as subduction occurred along the margins of Northeast Asia and northwestern part of the North American Cordillera. (2) From about the Late Triassic through the mid-Cretaceous, a succession of offshore island arcs and tectonically paired subduction zones formed near continental margins with subsequent accretion and substantial growth of the North Asian and North American continents. (3) From about mainly the mid-Cretaceous through the Present, a succession of igneous arcs and tectonically paired subduction zones formed along the continental margins. (4) From about the Jurassic to the Present, oblique convergence and rotations caused orogen-parallel sinistral and then dextral displacements within the upper plate margins of Northeast Asia and the North American Cordillera. (5) From the Early Jurassic through Tertiary, movement of the upper continental plates towards subduction zones resulted in strong plate coupling and accretion of the former island arcs and subduction zones to continental margins. Accretions were accompanied and followed by crustal thickening, anatexis, metamorphism, and uplift. And (6), in the middle and late Cenozoic, oblique to orthogonal convergence between the Pacific Plate, with respect to Alaska and Northeast Asia, resulted in formation of the modern-day ring of volcanoes around the Circum-North Pacific. Oblique convergence between the Pacific Plate and Alaska also resulted in major dextral-slip faulting in Alaska and the northern Canadian Cordillera, and along the western part of the Aleutian-Wrangell arc. 2000-05 Scotese, C.R., Scholl, D.W., Khanchuk, A.I., Monger, J.W.H., Dawson, K.M., Norton, I.O., Perfenov, L.M., and Stone, D.B., 2000. Interactive demonstration of dynamic computer model for the Phanerozoic tectonic and metallogenic evolution of the Circum-North Pacific, Geological Society of America, Cordilleran Section and associated societies, 96th annual meeting, Abstracts with Programs, v. 32, issue 6, p. 67. does this match? Abstract: Computer morphing of a series of fourteen time-stage diagrams for the tectonic evolution of the Circum-North Pacific is used to produce a continuous-action, dynamic computer model. The model, that is based on a geologic and tectonic analysis of the region, illustrates the complex Phanerozoic tectonic and metallogenic evolution of the region, and permits recognition of major events and interactions that are not easily perceived in viewing a series of static diagrams. The major tectonic and metallogenic events illustrated in the model are as follows. (1) In the Late Proterozoic, and Late Devonian and Early Carboniferous, major periods of rifting occurred along the margins of Northeast Asia and northwestern part of the North American Cordillera. (2) From the Late Triassic through the mid-Cretaceous, a succession of island arcs and tectonically paired subduction zones formed near continental margins. (3) From the mid-Cretaceous through the Present, a succession of igneous arcs and tectonically paired subduction zones formed along the continental margins. (4) From the Jurassic to the Present, oblique convergence and rotations caused orogen-parallel sinistral and then dextral displacements within the upper plate margins of Northeast Asia and the North American Cordillera. (5) From the Early Jurassic through Tertiary, movement of the upper continental plates towards subduction zones resulted in strong plate coupling and accretion of the former island arcs and subduction zones to continental margins. Accretions were accompanied and followed by crustal thickening, anatexis, metamorphism, and uplift. Finally (6) in the middle and late Cenozoic, oblique to orthogonal convergence between the Pacific Plate, with respect to Alaska and Northeast Asia, resulted in formation of the modern-day ring of volcanoes. 2000-06 Boucot, A.J., Chen, Xu, and Scotese, C.R., 2000. Phanerozoic paleogeographic revisions suggested by climatic and biogeographic information, Brazil 2000, 31st International Geologic Congress, International Geologic Congress Abstracts, Vol. 31. Abstract: Our compilation of climatically sensitive data (evaporites, calcretes, tillites, dropstones, glendonites, coals, bauxite, kaolin, laterites, etc. ), Cambrian through Miocene, permits us to recognize climatic belts for 26 time intervals. When added to certain biogeographic information this permits us to substantially revise paleogeographies, particularly those of the earlier and middle Paleozoic. We have, to date, accumulated over 7,000 data points derived from about 4,000 references and other sources. From the Cambrian through the Middle Devonian our data is compatible with the continents all being in the Southern Hemisphere, except for the low northern latitude Siberian Platform. Beginning in the later Devonian Laurentia, Baltica, and adhering continents, begin to move northwards. By the Mississippian much of Laurentia and Baltica are in the Northern Hemisphere. In the Pennsylvanian, Permian and post- Paleozoic our reconstructions do not differ substantially from those suggested by many others. A number of changes have been made in the varied East Asian blocks and terranes to be in concord with our biogeographic and climatic information. Laurentia in the Cambrian is situated with its southern, Ouachita margin, including the adjacent Precordilleran Terrane of western Argentina, adjacent to west-central South America. Beginning in the Middle Ordovician Laurentia begins to move east relative to western South America, until by the Early Devonian it reaches approximately its present position to the north of Colombia and Venezuela. Most of Mexico, south of the Mojave-Sonora Megashear is envisioned as an integral part of South America through the Silurian. After substantially more climatic and biogeographic information are gathered we anticipate still more paleogeographic changes, but not of a major character. 2000-07 Scotese, C.R., 2000. “Pangea”, article for print and electronic versions of Encyclopedia Britannica. (82) 2000-08 Nokleberg,W.J., Parfenov, L.M., Monger, J.W., Norton, I.O., Khanchuk, A.I., Stone, D.B., Scotese, C.R., Scholl, D., and Fujita, K., 2000. Phanerozoic tectonic evolution of the Circum-North Pacific, U.S. Geological Survey Professional Paper 1626, 122 pp. (88) add abs? 2000-09 Scotese, C.R., 2000. “Gondwana”, article for print and electronic versions of Encyclopedia Britannica. (84) 2000-10 Scotese, C.R., and Schettino, A., 2000. A Synthetic APWP for Africa (Jurassic-Present) and Global Plate Tectonic Reconstructions, American Geophysical Union 2000 Spring Meeting, EOS, Transactions of the American Geophysical Union, v. 81, issue 19, p. 180 2000-11 Scotese, C.R., 2000. Mesozoic paleoglobes on p. 50, in John Flynn, Monsters of Madagascar: Digging into the past, National Geographic Magazine, August, 2000, vol. 198, number 2, p. 46-51, National Geographic Society, Washington, D.C. 2000-12 Scotese, C.R., 2000. Permian paleogeographic map on p. 103, in Hillel J. Hoffman, When Life Nearly Came to an End: The Permian Extinction, National Geographic Magazine, September, 2000, vol. 198, number 3, p. 100-113, National Geographic Society, Washington, D.C. 2000-13 Scotese, C.R., 2000. Late Jurassic paleogeographic map on p. 24, in Barbara Eaglesham, Silent Messengers of Gondwana, Odyssey: Adventures in Science, September, 2000, volume 9, number 6, Cobblestone Publishing, Petersborough , NH. 2000-14 Metz, K.S., and Scotese, C.R., 2000. A test of the snowball Earth hypothesis using lithologic indicators of climate, Geological Society of America 2000 Annual Meeting, Abstracts with Programs, v. 32, issue 7, p. 385. add Metz thesis Abstract: The Snowball Earth (SBE) hypothesis proposes that during Marinoan time in the late Proterozoic, 640-600 m.y., the Earth's continents and the surface of the oceans were covered with glaciers and ice, and the Earth resembled a giant snowball. Eventually, the carbon dioxide concentration increased due to volcanic activity producing global warming and the deposition of cap carbonates immediately above the glacial deposits. The SBE hypothesis makes several testable predictions: 1) there should be no well-defined climatic zones, 2) tillites should be equally abundant at tropical and temperate latitudes, and 3) cap carbonates, also, should occur at any latitude. In order to test these predictions, we have collected lithologic indicators of climate from more than 350 localities worldwide. Lithologic and environmental data were collected for the interval between 750 and 550 mya. These data were assembled as an ArcView GIS project and plotted on 5 paleogeographic and paleotectonic reconstructions based on paleomagnetic evidence. The goal was to determine, 1) if the climate was zonal or azonal, 2) if tillites commonly occurred at tropical latitudes, and 3) if cap carbonates occurred at high latitudes. A statistical test of zonality was performed using the method of Scotese and Barrett (1988). Preliminary results indicate that there were distinct tropical and temperate zones throughout the 200 million year interval of the late Proterozoic. Though some tillites are found in tropical latitudes, the majority are found in temperate and polar latitudes. Cap carbonates, on the other hand, commonly occur at high latitudes, which supports the suggested rapid transition from Ice House to Hot House conditions. 2000-15 Scptese, C.R., 2000. Late Carboniferous map in Venture Across America, #102 Illinois: “Tully Monster” - Equatorial Creatures in Grundy County, UHaul Advertisement. 2000-16 Scotese, C.R., 2000. http://www.scotese.com in Web Watch, Physics Today, September, 2000, p. 58. Abstract: Geologist Christopher R. Scotese, who's based at the University of Texas at Arlington, is the creator of the Paleomap Project, a Web site devoted to illustrating the plate tectonic development of the Earth's continents and ocean basins. Among the site's many animations is one that shows how continental configuration will change of the next 250 million years. 2001 2001-01 Boucot, A.J., C. Xu and Scotese, C.R., 2001. Changing positions of Phanerozoic climatic belts and accompanying paleogeographic changes. International Symposium on exploring the history of life on the Earth, Paleontology in China during the last 15 years. National Natural Science Foundation of China, pp. 53-57. (91) 2001-02 Schettino, A. and Scotese, C.R., 2001. New Internet software for paleomagnetic analysis and plate tectonic reconstructions, EOS, Transactions of the American Geophysical Union, v. 82, issue 45, p. 530, 536. (89) no abs 2001-03 Scotese, C.R., Nokleberg, W.J., Monger, J.W., Norton, I.O., Parfenov, L.M., Khanchuk, A.I., Bundtzen, T.K., Dawson, K.M., Eremin, R.A., Frolov, Y.F., Fujita, K., Goryachev, N.A., Pozdeev, A.I., Ratkin, V.V., Rodionov, S.M., Rozenblum, I.S., Scholl, D.W., Shpikerman, V.I., Sidorov, A.A., and Stone, D.B., 2001. Dynamic computer model for the metallogenesis and tectonics of the Circum-North Pacific, Open File Report - U.S. Geological Survey, OF 01-0261. also 01-262? (87) This document describes the digital files on this CD- ROM report that consists of a dynamic computer model of the metallogenesis and tectonics of the Circum-North Pacific, and background articles, figures, and maps. The CD-ROM report is for sale by U.S. Geological Survey, Information Services, ESIC Open-File Reports, PO Box 25286, Denver, CO 80225 (Telephone 888-ASK- USGS). The tectonic part of the dynamic computer model on this CD-ROM is derived from a major analysis of the tectonic evolution of the Circum-North Pacific (Nokleberg and others, 2001) which is also contained on this CD-ROM in directory \tectevol. The dynamic computer model and associated materials on this CD-ROM are part of a project on the major mineral deposits, metallogenesis, and tectonics of the Russian Far East, Alaska, and the Canadian Cordillera. The project provides critical information on bedrock ge&logy and geophysics, tectonics, major metalliferous mineral resources, metallogenic patterns, and crustal origin and evolution of mineralizing systems for this region. The major scientific goals and benefits of the project are to: (1) provide a comprehensive international data base on the mineral resources of the region that is the first, extensive knowledge available in English; (2) provide major new interpretations of the origin and crustal evolution of mineralizing systems and their host rocks, thereby enabling enhanced, broad-scale tectonic reconstructions and interpretations; and (3) promote trade and scientific and technical exchanges between North America and Eastern Asia. 2001-04 Scotese, C.R. and de Wit, M., 2001. Gondwana’s story: A Tale of Tectonic and Climatic Change, In Gondwana Alive (in press, submitted July, 2000). (90) what is going on with this? no abs 2001-05 Boucot, A.J., C. Xu and C.R. Scotese, 2001. Changing positions of Phanerozoic climatic belts and accompanying paleogeographic changes. Pages 11-12 in Evolutsiya zhizni na zemle, Materiali II Mezhdunarodnogo Simposyma, Tomsk Gosudarstnogo Universitet. (92a) no abs 2001-06 Scotese, C.R., 2001. Atlas of Earth History, Volume 1, Paleogeography, PALEOMAP Project, Arlington, Texas, 52 pp (86). 2001-07 Scotese, C.R., 2001. 3D Paleotopographic and Paleobathymetric Reconstructions for the Early and Late Miocene, American Geophys. Union, Spring Meeting, Boston. XXXX 2001-08 Scotese, C.R., 2001. Triassic, Jurassic, and Cretaceous paleogeographic maps on p. 89, in Richard Monastersky, The Rise of Life on Earth: Pterosaurs, Lords of the Ancient Skies, National Geographic Magazine, May, 2001, vol. 199, number 35, p. 86-105, National Geographic Society, Washington, D.C. b no abs 2001-09 Metz, K., and Scotese, C.R., 2001 Late Proterozoic plate tectonic and paleo-environmental reconstructions: Implications for the snowball Earth hypothesis, Earth System Processes - Global Meeting, Edinburgh, Scotland (June 24-28, 2001), Geological Society of America and Geological Society of London, Program with Abstracts, p. 125. Abstract: Plate tectonic and paleo-environmental reconstructions have been produced for 5 time intervals during the Late Proterozoic (750 - 550 Ma). During this time interval the supercontinent of Rodinia rifted apart and reassembled to form a new supercontinent, Pannotia. These reconstructions show the inferred location of active plate boundaries, the sequence of Pan-African collisions that formed Gondwana - the core continent of Pannotia, as well as the approximate distribution of deep ocean basins, shallow seas, lowlands, and mountainous areas. The plate tectonic reconstructions were produced by working backwards from well constrained early Cambrian reconstructions, using sparse but internally consistent paleomagnetic results from North America, Africa, and Australia, carefully considering the timing of tectonic events, employing the principle of "minimum surprise" and eschewing true polar wander. The paleo-environmental interpretations are based on a global compilation of chronologic, stratigraphic, lithologic, environmental, and paleoclimatic information from over 350 late Proterozoic localities. Particular attention was paid to the occurrence of lithologic indicators of climate such as tillites, evaporites, and carbonates. Form our study we conclude that Rodinia, much like the late Paleozoic Pangea, stretched from the North Pole to the South Pole. Pannotia, on the other hand, was primarily a southern hemisphere supercontinent, centered on the South Pole. Speculative, late Proterozoic reconstructions that show the continents arrayed along the equator are untenable. The late Proterozoic was an Ice House world. The low latitude, Himalayan-sized Grenvillian and Pan-African mountain ranges that crossed the centers of Rodinia and Pannotia, respectively, may have promoted these Ice House conditions. Regarding the "Snowball Earth" hypothesis, we find that the distribution of tillites indicates that there were distinct tropical and temperate zones throughout the entire 200 million year interval. Using the method of Scotese and Barrett (1988), it was determined that these zones are statistically significant. Though some tillites are found in tropical latitudes, the majority are found in temperate and polar latitudes. Cap carbonates, on the other hand, appear to occur at all latitudes. 2001-10 Scotese, C.R., 2001. 3D paleogeographic reconstructions of the late Paleozoic continents and ocean basins, Earth System Processes - Global Meeting, Edinburgh, Scotland (June 24-28, 2001), Geological Society of America and Geological Society of London, Program with Abstracts, p. 102. Abstract: Plate tectonic, paleogeographic and paleoceanographic events during the Late Paleozoic may have transformed the Earth from a Hot House to Ice House world. In order to better understand the changing world of the Late Paleozoic, five, 3D paleogeographic models were built that illustrate the paleotopography of the continents and a speculative paleobathymetry of the Late Paleozoic ocean basins. 3D paleoglobes have been made for the Late Devonian (Famenian, 360 Ma), Early Carboniferous (Visean, 340 Ma), mid-Carboniferous (Namurian, 320 Ma), Late Carboniferous (Moscovian, 300 Ma), and Early Permian ( Sakmarian, 280 ma). During the Late Devonian, a pre-Pangea had begun to assemble in the southern hemisphere. North America was in collision with northern South America, and the ocean basins between Europe and North Africa had nearly disappeared. Paleotethyan ocean basins, however, still separated Siberia from the Kazakhstan island arcs, and a wide ocean lay between the Cathaysian continents (N. &S. China) northern hemisphere continents. During the early Carboniferous (Tournaisian-Visean), pre-Pangea rotated northward. The Canadian Arctic moved from an equatorial position to a subtropical latitude, and the still emergent Caledonian and Northern Appalchians moved into the equatorial rainy belt. Siberia and the island arcs of Kazakhstan had begun to coalesce, and the Cathaysian continents (North and South China), separate from Gondwana, were in transit across PaleoTethys. By the mid-Carboniferous (Namurian B), western Pangea had assembled. The rising, equatorial, Central Pangean Mountains separated North America and Europe from the Gondwana continents. Kazakhstania and Siberia were in collision, and North China, with South China in tow, was beginning to collide along the Tien Shan range of southern Kazakhstan. Through the mid and late Carboniferous, and into the earliest Permian, convergence and mountain building continued the consolidation of western Pangea. The paleotography and paleobathymetry of the Late Paleozoic world has been modelled using inexpensive, 3D rendering software (Amorphium). These 3D elevation models have a vertical resolution of 40 meters, and geographic resolution of approximately 10 km. 2001-11 Scotese, C.R., 2001. Times of global plate tectonic reorganization and their causes, Earth System Processes - Global Meeting, Edinburgh, Scotland (June 24-28, 2001), Geological Society of America and Geological Society of London, Program with Abstracts, p. 69. Abstract: The plate tectonic history of the Earth is the foundation upon which all other components of the Earth System must rest. Since 1985, the PALEOMAP Project has been assembling a global, plate tectonic model that describes the motions of the continents and evolution of the ocean basins during the last 1100 million years. Jurassic, Cretaceous and Cenozoic plate motions are based on linear magnetic anomalies, the tectonic fabric of the ocean floor revealed by satellite altimetry, and the absolute motion trajectories determined by Indian and Atlantic hotspot tracks. Early Mesozoic, Paleozoic and Late Precambrian plate tectonic reconstructions are based on paleomagnetic data, lithologic indicators of climate, biogeographic inferences, and the timing of continental rifts and collisions. The author has synthesized these diverse and complementary datasets, to produce a global, finite rotation model that describes the movement of over 500 tectonic elements and terranes. This model of Phanerozoic and Proterozoic plate motions permits quantitative estimates of the changes in the plate velocity, and can be used to identify times of major plate reorganization. A preliminary analysis of the PALEOMAP global plate model has identified at least 12 times of global plate reorganization. They are (in millions of years): 1100, 750, 570, 400, 320, 300, 210, 170, 140, 90, 75, 50. What causes global plate tectonic reorganizations? Numerous authors have suggested that mantle plumes or hotspots may initiate supercontinent breakup. We, however, propose that most significant plate tectonic reorganizations are caused by fundamental changes in plate boundaries that result in new lithospheric stresses. The two principle mechanisms are: continent-continent collision and the progressive subduction of a major oceanic ridge. Plate reconstructions showing the location, or inferred location (pre-Jurassic), of spreading centers, subduction zones, and areas of continental collision will be presented for the 12 time intervals of global plate reorganization. 2001-12 Scotese, C.R., 2001. Evolution: Change Through Time Poster, supplement to Eos, Transactions, American Geo[physical Union, volume 82, number 36, September 4, 2001, Washington, D.C. no abs 2001-13 Scotese, C.R., 2001. Paleogeographic maps on p. 47, in M.J. Smith and J.B. Southard, Exploring the evolution of plate tectonics, Science Scope, volume 25, number 1, National Science Teachers Association (NAST), Arlington, VA. no abs 2001-14 Scotese, C.R., 2001. Late Precambrian and Early Paleozoic, Paleogeographic, Plate Tectonic, and Paleoclimatic Reconstructions, (poster), Early Palaeozoic Palaeogeography and Palaeobiogeography of Western Europe and North Africa, Lille, France, (September 24-26) 2001-15 Scotese, C.R., 2001. Animation of Plate Motions and Global Plate boundary Evolution since the Late Precambrian, Geological Society of America 2001 Annual Meeting, Boston, (November 2–6), Abstracts with Programs, v. 33, issue 6, p.85. Abstract: A computer animation will be presented that illustrates both plate motions and the evolution of plate boundaries since the Late Precambrian. Plate motions during the Jurassic, Cretaceous and Cenozoic plate motions are based on linear magnetic anomalies and the tectonic fabric of the ocean floor revealed by satellite altimetry, in combination with "absolute" motion trajectories determined by the Indian and Atlantic hotspot tracks and paleomagnetism. Early Mesozoic, Paleozoic and Late Precambrian plate tectonic reconstructions, however, are less well constrained and are based on less precise paleomagnetic data, lithologic indicators of climate, biogeographic inferences, and the timing of continental rifts and collisions. In addition to the motion of the plates, the animation shows the continuous evolution of global plate boundaries. Though the rifts and subduction zones associated with the breakup of Pangea are well known, the pre-Mesozoic plate boundaries shown here are speculative. Their location is based on the timing of rifts and continental collisions inferred from the geologic record, and the fundamental assumption that plates move as a result of slab pull and ridge push. For example, fast moving plates must be attached to old, cold subducting slabs. Large continental plates (Eurasia), on the other hand, tend to move slowly because of deep lithospheric keels. The evolving geometry of plate boundaries controls the tempo and mode of plate evolution. The history of plate motions might be best described as "long periods of boredom, interrupted by short intervals of terror (rapid change)". Episodes of global plate reorganization punctuate long periods of steady-state plate motion. As shown by the animation, these global reorganizations are due to catastrophic changes in plate boundary geometry that result in new lithospheric stress regimes. One of the most important plate boundary events is the subduction of a spreading center. The subduction of the Tethyan Ridge in the early Jurassic may have been responsible for the breakup of Pangea. 2001-16 Scotese, C.R., and Dilek, Y., 2001. Animation of plate motions and ophiolite genesis through time, Geological Society of America 2001 Annual Meeting, Boston, (November 2–6), v. 33, issue 6, p. 171. Abstract: A computer animation is presented that illustrates past plate motions, the evolution of major plate boundaries, and the origin and emplacement of over 200 ophiolite complexes. Plate motions during the last 150 million years are based on linear magnetic anomalies and the tectonic fabric of the ocean floor revealed by satellite altimetry, in combination with "absolute" motion trajectories determined by the Indian and Atlantic hotspot tracks and paleomagnetism. Pre-Mesozoic plate motions, however, are less well constrained and are based on less precise paleomagnetic data, lithologic indicators of climate, biogeographic inferences, and the timing of continental rifts and collisions. In addition to the motion of the plates, the animation shows the continuous evolution of global plate boundaries, the locations of ophiolite formation, and the locations of ophiolite emplacement during times of continent-continent, and continent-arc collision. The computer animation is based on the PALEOMAP finite rotation model that describes the movement of over 500 plates and terranes since the Late Precambrian. The ophiolite database compiled by the authors records the present-day latitude/longitude of each ophiolite locality as well as the igneous and tectonic environment of origin, age and mode of tectonic emplacement, the source of the information, reliability codes for the age of origin and emplacement, as well as relevant petrologic characteristics. The purpose of the animation was to both show the history of ophiolites in a plate tectonic framework, as well as answer fundamental questions concerning the tempo and mode of ophiolite formation and emplacement. Are most ophiolites formed at mid-ocean ridges or in suprasubduction zone environments? How long after formation at spreading centers are ophiolites emplaced? Is there any spatial or temporal pattern to ophiolite formation and emplacement? These are fundamental questions that have led to different controversies in the evolution of the ophiolite concept through time. Preliminary analysis of the animation suggests that both the age of origin and the age of emplacement of ophiolites are not random, but clustered, episodically. The timing of "ophiolite events" appears to be closely related to times of global plate reorganization. also ppt 2001-17 Burkart, B., and Scotese, C.R., 2001. Cenozoic rotation of the Yucatan (Maya) block along the Orizaba Fault Zone of Southern Mexico, the Faults of Central America, and the Cayman Trough, Geological Society of America 2001 Annual Meeting, Boston, (November 2–6), Abstracts with Programs, v. 33, issue 6, p.154. Abstract: Yucatan (Maya) has been an independent block since early Cenozoic when counter-clockwise rotation began that continues today. It is bounded in Mexico by the Orizaba fault zone (OFZ), which begins near the Gulf of Mexico at the Santa Ana massif, runs along the western Isthmus of Tehuantepec, crosses the northern Gulf of Tehuantepec W of the Chiapas massif, and connects with the major faults of Guatemala and the Cayman trough. Faults of Guatemala and adjacent Honduras are boundaries to wedges whose eastward rotation has been away from the Cuicateco terrane of Oaxaca, Mexico. Dextral slip of about 340 km across the OFZ is measured by offset of Laramide structures and Mesozoic and Tertiary contacts of the northern Chiapas massif from those in the fold and thrust belt of the Sierra Madre Oriental. Reversing the Cenozoic counter-clockwise rotation and simultaneously restoring previously-known sinistral offset across the Polochic fault of 130 km, moves the westernmost part of the tapered block between the Polochic and Jocotan faults (Chuacus-Tambor block) of Guatemala to a position between the Yucatan and Guerrero blocks about 160 km NW of the Pacific coast. Very little offset occurred across the Motagua fault zone. The northernmost part of the Chiapas massif is moved NW across the Isthmus to near the Santa Ana uplift near the Gulf of Mexico. Ophiolites, granitoids, metasedimentary rocks and volcaniclastics related to Cretaceous arc magmatism found in the Cuicateco terrane of Oaxaca and Tambor of Guatemala are juxtaposed with this restoration model. Obduction during strike-slip movement may account for wider distribution of ophiolites of Guatemala, which were obducted during strike-slip movement. The eastern Veracruz basin opened during rotation of the Yucatan block. Sinistral offset across the Chiapas Strike-Slip fault zone may reflect partial decoupling from the rest of the Yucatan block. The western basin (Cordoba platform) was dropped downward at an early stage of rotation. 2001-18 Scotese, C.R., 2001. Rodinia Map on p. 148, in Marc J. Defant, Natural Science, Science Essay: Ice Over Earth, The World & I, November, 2001, published by the Washington Times Corporation, Washington, D.C. no abs 2001-19 Scotese, C.R., 2001. Paleogeographic map of Europe on p. 17, in Gretchen Noyes-Hull, Making Mountains: The Medieval and Modern Geology of Leonardo da Vinci, Odyssey: Adventures in Science, November 2001, Cobblestone Publications, Petersborough, NH. no abs 2001-20 Scotese, C.R., 2001. Animation: Ophiolites Through Time (Ophiolites.mov, Quicktime format), PALEOMAP Project, www.scotese.com, Evanston, IL. 2002 1) restart PALEOMAP Project Consortium 2002-01 Nokleberg, W.J., Scotese, C.R., Bundtzen, T.K., Parfenov, L.M., Monger, J.W., Dawson, K.M., Khanchuk, A.I., Shpikerman, V.V., Goryachev, N.A., Stone, D.B., and Norton, I.O., 2002. Dynamic computer model for metallogenesis and tectonics of the Cicum-North Pacific, International Conference on Tectonics and Metallogeny of Central and Northeastern Asia, Rossiyskoy Akademii Nauk, Izdatel'stvo Sibirskoye Otdeleniye ; Novosibirsk, 23 pp. 2002-02 Schettino, A. and Scotese, C.R., 2002. Global Kinematic constraints to the tectonic history of the Mediterranean region and surrounding areas during the Jurassic and Cretaceous, Journal of the Virtual Explorer, v. 8, pp. 149-168. URL: http://virtualexplorer.earth.monash.edu.au/VEjournal/2002/Rosenbaum/contents.html, ,http://virtualexplorer.com.au/VEjournal (92b) Abstract: The formation of small fragments of continental lithosphere, which rift away from a passive margin and are carried toward a trench together with the surrounding oceanic crust, is a characteristic of many collisional settings, in particular of the northern margin of Gondwana during the Mesozoic. This motion, though chaotic appearance, can be described rigorously in terms of plate kinematics driven by local temporal variations in the relative velocity field between the main colliding plates. In this model proposed here, the rifted continental fragments approach the trench with the same stationary velocity as the oceanic lithosphere in which they are embedded, while the spreading centers that separate these microplates from the rifted continental margin, either speed up or slow down in order to compensate for small variations of the velocity field between the major colliding plates. Hence, the oceanic leading edge of a subducting plate may separate from its continental part and move independently to ensure a constant convergence rate at the trench. The application of this principle to the complex tectonic history of the Mediterranean region during Jurassic and Cretaceous times is performed starting from a revised global plate motion model. A set of maps illustrating the regional velocity and acceleration fields is presented for nine major phases from the Bajocian through the Maastrichtian. These maps provide new constraints that may be helpful for the construction of plate tectonic models of the Tethyan realm. New insights into some of the major tectonic events that occurred during the Jurassic and the Cretaceous in the Mediterranean region are gained from the correlation between kinematic events and geologic evidence. 2002-03 Nokleberg, W.J., Scotese, C.R., Bundtzen, T.K., Parfenov, L.M., Monger, J.W., Dawson, K.M., Khanchuk, A.I., Goryachev, Shpikerman, V.V., and Norton, I.O., 2002. Dynamic computer model for the metallogenesis and tectonics of the Circum-North Pacific, AAPG Pacific Section and SPE Western Region Conference, AAPG Bulletin, v. 86, issue 6, p. 1155. Abstract: The metallogenic and tectonic development of the Circum-North Pacific (Russian Far East, Alaska, Canadian Cordillera, and adjacent offshore areas) is illustrated in a dynamic computer model that portrays the formation of a series of metallogenic belts. The Phanerozoic metallogenic and tectonic evolution of the Circum- North Pacific (Russian Far East, Alaska, and the Canadian Cordillera) is recorded in the cratons, craton margins, and orogenic collages of the Circum-North Pacific mountain belts that separate the North Pacific from the eastern North Asian and western North American Cratons. The collages consist of tectonostratigraphic terranes with older metallogenic belts that are composed of fragments of igneous arcs, accretionary-wedge and subduction-zone complexes, passive continental margins, and cratons; they are overlapped by continentalmargin-arc and sedimentary-basin assemblages with younger metallogenic belts. The metallogenic and geologic history of terranes, overlap assemblages, cratons, and craton margins is highly complicated because of post-accretion dismemberment and translation during strike-slip faulting that occurred subparallel to continental margins. 2002-4 Scotese, C.R., 2002. 3D paleogeographic and plate tectonic reconstructions: The PALEOMAP Project is back in town, presented at Houston Geological Society International Exploration Dinner Meeting, Houston, TX, May 20, 2002, The Bulletin of the Houston Geological Society, v. 44, issue 9, p. 13-15. The PALEOMAP Project is known for its synthesis of the plate tectonic, paleogeographic, and paleoclimatic history of ocean basins and continents during the last 1,100 million years, and the illustration of Earth history through maps, computer animations, and Geographic Information Systems (GIS). In this talk, Chris will present his latest 3D paleogeographic and plate tectonic maps and animations (see cover illustration of Paleo Topography and Bathymetry of the Late Cretaceous 80 MYA). Global plate tectonic, paleogeographic and paleoclimatic reconstructions will be presented for the early Miocene, Late Cretaceous, Permian, and Devonian. These reconstructions use 3D paleotopographic and paleobathymetric information to represent the surface of the Earth and the shape and depth of the ocean basins. Each map is composed of over 6 million pixel- points that capture digital elevation information at a 10 X 10 km geographic resolution and 40 meter vertical resolution. This quantitative, digital approach to paleogeographic modeling permits new ways to visualize and analyze the changing surface of the Earth through time using standard GtS (ESR1 3D Analyst, Spatial Analyst), 3D modeling, and computer animation techniques. The process of building a 3D paleogeographic map begins with the digital topography and bathymetry compiled by NOAA, the BEDMAP Project, and the IBCAO Arctic Project. The topographic and bathymetric information is gridded at a 6-minute resolution, and the individual data points (pixel-points) are rotated back to their paleopositions using the global plate tectonic model of the PALEOMAP Project. The resulting map is reconstruction of present-day bathymetry and topography in paleo-coordinates (late Miocene, Figure 1). In the next processing steps, the digital elevation and bathymetric values are corrected to take into account the complex effects of thermal subsidence, glacial rebound, tectonic and volcanic activity and erosion. The result is a revised global paleotopographic and paleobathymetric surface. To complete the 3D paleogeographic model the new topographic surface is digitally “flooded” by raising or lowering sea level according to the estimates from eustatic sea level curves. The new paleogeographic map raises interesting geological questions. For instance, the shorelines shown in the early Miocene map (Figure 2) are familiar but not identical to today’s coastlines. Florida is flooded, as are the molasse basin of the Alps, the Persian Gulf foredeep and the peri-Caspian region. But surprisingly, so are the Amazon and Parana basins. Conversely, if sea level were higher, one might expect that Southeast Asia would be flooded. However, geologic evidence indicates that Southeast Asia was emergent during the early Miocene. This suggests that dynamic plate tectonic forces associated with subduction in the Java-Sumatra trench may be “pulling-down” the leading edge of Indonesia. The digital topographic and bathymetric models presented here are currently being used for paleoclimatic and paleoceanographic simulations. They provide the framework and foundation for a detailed and quantitative modeling of Earth surface processes since the late Precambrian. 2002-05 Grossman, E.L., Pollard, D., Scotese, C.R., and Hyde, W.T., 2002. Oxygen isotope and global climate model (GCM) investigations of Permo-Carboniferous climate, Geological Society of America 2002 Annual Meeting, Abstracts with Programs, v.34, issue 6, p. 501. (92c) Abstract: Oxygen isotopes in Carboniferous and Early Permian brachiopod shells from North America and the Russian Platform show up to 3 per mil variations suggestive of greenhouse-icehouse-greenhouse transitions. To evaluate the paleoclimatic significance of these temporal trends as well as interregional oxygen-isotope differences, we simulated Late Paleozoic climate (360, 320, and 280 Ma) utilizing the GENESIS v. 2.0 GCM. Paleogeographies are modified from Scotese et al. (1999, J. African Earth Sci. 28:99) with topographies inferred from tectonic relationships. The model was run with 1x and 4x modern preindustrial pCO2 levels (280 ppm) for each time interval. During most of the Mississippian, the U. S. mid-continent (USM) was traversing the subtropical high of the Southern Hemisphere. By the mid-Carboniferous, the area had entered the ITCZ, and remained in the tropics through the Early Permian. Oxygen isotope data for brachiopod shells reflect in part this transit across climate zones. For the U. S. mid-continent, low oxygen isotopic values in the earliest Mississippian give way to high values in the mid-Mississippian. The delta O18 values decrease in the Late Mississippian, coinciding with the transition to wet, tropical climate. A delta O18 increase at or near the mid-Carboniferous boundary cannot be explained by precipitation-evaporation variations and is likely caused by decreasing temperatures and increasing ice volume. During the Permo-Carboniferous, the Russian Platform transited from the tropics to the subtropics. Rather than showing a delta O18 increase that might correspond to a progressive increase in salinity, the oxygen isotopic record shows variation on a roughly 20 m.y. time scale that likely reflects ice volume change. This includes a sharp Mid-Carboniferous delta O18 increase that coincides with the delta O18 increase in North America, further suggesting a transition from greenhouse to icehouse conditions. Oxygen isotope estimates of paleotemperature show good agreement with GCM results for some intervals (i.e., the earliest Pennsylvanian), but not for others (e.g., the latest Mississippian). Potential causes for this disagreement (e.g., inaccurate data or incorrect pCO2 estimates) are being investigated. These results demonstrate the utility of coupling climate model and isotopic studies of Paleozoic climate. 2002-06 Chatterjee, S., and Scotese, C.R., 2002. Evolution and biogeography of the Indian Plate since the Cretaceous, Geological Society of America 2002 Annual Meeting, Abstracts with Programs, v.34, issue 6, p. 315. Abstract: The evolution of the Indian plate after its breakup from Gondwana and its subsequent collision with Asia is one of the most profound, violent, and complex events in plate tectonics and geodynamics, marked by volcanism, impact and mountain building. A new model for the tectonic evolution of the Indian plate recognized a missing landmass, called Greater Somalia that occupied a position between eastern Arabia and northwestern India. Throughout most of the Cretaceous, India was separated from the rest of Gondwana, but in the latest Cretaceous it reestablished contact with Africa through Greater Somalia, allowing immigration of dinosaurs and other vertebrates from Africa and Europe. The Somalia connection solves the riddle of Indian biogeography—the lack of endemism among Indian Maastrichtian dinosaurs and other vertebrates. During its tumultuous journey for the last 145 million years, India rifted from Gondwana below the equator and traveled some 5,000 km northward across the Tethys to collide with Asia. Along its journey, it was punctured by the Rajmahal and the Deccan hotspots on its eastern and western margins during the Early and Late Cretaceous respectively, creating spectacular continental flood basalt provinces, while leaving hotspot trails on its two sides along the Indian Ocean. Between these two thermal events, the Marion hotspot initiated sea-floor spreading in the Mascarene basin around 88 Ma, resulting in the separation of Madagascar and India. About 65 million years ago, the Indian plate was severely battered by a giant asteroid on its passive western margin, creating the enormous Shiva Crater on the Mumbai Offshore Basin. The submerged Shiva crater, buried by 5 km of postimpact Tertiary sediments, is about 600 km long and 400 km wide, and is considerably larger than the Chicxulub. At the impact, the Carlsberg Ridge jumped 500 km north from the Mascarene Basin to separate the Seychelles from India. At the same time, the impact triggered the main pulse of the of the Deccan volcanism. The interaction of impact with the Carlsberg Ridge may have generated spreading asymmetry associated with India's sudden northward acceleration at rates more than 16 cm/year. The velocity of the Indian plate motion dropped considerably to 8 cm/year during the Eocene (50 Ma), marking the initial collision with Asia. 2002-07 Scotese, C.R., 2002. Paleogeography: locating the best seafood through time, Geological Society of America 2002 Annual Meeting, Abstracts with Programs, v.34, issue 6, p. 542. Abstract: Why stay at home and cook, when you can go out to eat? The choice to eat out, however leads to the inevitable and perennial questions, "What should we eat?" and "Where should we go?". Taking the advice of Dr.Richard K. Bambach, I would recommend "seafood". Seafood contains many of the vitamins and minerals necessary to sustain an active life, it is often proffered in environments that are attractively and unusually decorated, and it tastes good! O.K., so seafood it is. Now, the tough and still unresolved question, “Where should we go to eat?". There are options. After all, marine environments serving seafood do vary: intertidal, shallow shelf, deep shelf, slope, rise, black smokers, abyssal ocean, even the occasional deep oceanic trench. I would avoid "Black Smokers"--no nonsmoking section, and instead would recommend the "Shallow Shelf". The "Shallow Shelf" has a diverse variety of entrees, which are constantly changing through time and the critters themselves are not unattractive. (For really ugly, but tasty, dining check out the "Abyssal Ocean".) However, if you find that what you want isn't on Shallow Shelf's menu, you can always leave and head for the "Deep Shelf”. As Dr. Bambach points out, you might get lucky and find it there. But where is the "Shallow Shelf". I can't give you directions but I can make you a map. A special kind of map, in fact, called a "paleogeographic map". A good paleogeographic map shows not only the locations of the ocean basins and continents, but also the location of highlands, lowlands, deep ocean basins, and you guessed it--the shallow shelf. You'll need a paleogeographic map because the continents keep moving and sea level keeps changing. What was once land might become shallow shelf, or shallow shelf might become land, deep shelf or even a mountain range. It's very confusing. Well, I hope you find your way. Bon appetit! 2002-08 Scotese, C.R., 2002. Paleogeographic constraints on biogeographic pathways, Geological Society of America 2002 Annual Meeting, Abstracts with Programs, v.34, issue 6, p. 316. Abstract. Paleogeographic maps provide the spatial context for understanding, interpreting and analyzing biogeographic patterns. A paleogeographic map, itself, is highly interpretive. On a global scale, a paleogeographic map must first represent the past positions of the continents and oceans according to the evidence from plate tectonics and paleomagnetism. However, this alone is not sufficient. Once the global plate tectonic framework has been established, a paleogeographic map must then illustrate the ancient distribution of highlands, lowlands, shallow seas, and deep ocean basins. This is done by reconstructing the changes in topography and bathymetry caused by tectonic and erosional processes. Young tectonic features, such as recent uplifts or volcanic eruptions, must be removed or reduced in size, whereas older tectonic features, such as ancient mountain ranges, must be restored to their former extent. As an example, ocean floor which subsides as it cools and moves away from a spreading ridge must be "unsubsided" or restored to its former depths. Once the ancient paleogeography is recreated, it is then possible to begin to model other global processes such paleoclimatic change, paleoceanographic circulation patterns, or changing biogeographic pathways. At the turn of the twentieth century, the unsuccessful attempts to explain ancient biogeographic patterns using modern geography were, in part, responsible for the formulation and acceptance of continental drift. At the turn of the twenty-first century, we are now poised to apply advances in plate tectonics, paleoclimatic modeling and paleoceanic circulation to produce a comprehensive set of paleogeographic maps that can be used to unravel some of the complex patterns of Phanerozoic biogeographic change. In this presentation a new set of 3D paleogeographic maps will be presented for the Phanerozoic and late Precambrian. 2002-9 Roest, W.R., Lee, S.K.Y., and Scotese, C.R., 2002. The changing surface of an active planet: Earth (poster), Geophysical Data Centre, Geological Survey of Canada, Ottawa, Ontario. no abs poster 2003 2003-01 Boucot, A.J., Rong Jia-Yu, Chen Xu, and Scotese, C.R., 2003. Pre-Hirnantian Ashgill climatically warm event in the Mediterranean Region, Lethaia , v. 36, issue 2, pp. 119-131. (94) Compilation of the marine, benthic megafossils from approximately the mid-Ashgill of the Mediterranean region, including much of Central and Southern Europe plus North Africa, and elsewhere indicates a warm interval featuring bioclastic limestone and a warm climate marine fauna. These mid-Ashgill faunas immediately precede the latest Ashgillian, Hirnantian, cool interval that featured widespread glaciation, and are underlain by typical, cold water, Mediterranean Realm, older Ordovician rocks and faunas. The cause or causes responsible for the brief warm interval are uncertain, but may have involved a warm water gateway that is geographically still not located. There is a possibility that South Africa was similarly affected by this roughly mid-Ashgillian marine situation. Early Paleozoic bauxite minerals and kaolins in northwestern Sudan and kaolins elsewhere in North Africa may represent the same time interval, which would suggest that there was a non-marine amelioration of the local climate as well as the marine effects. 2003-02 Nokleberg, W.J., Scotese, C.R., Bundzen, T.K., Parfenov, L.M., Monger, J.W., Dawson,K.M., Khanchuk, A.I., Shpikerman, V.I., Goryachev, N.I., and Stone, D.B., 2003. Dynamic computer model for metallogenesis and tectonics of the Circum-North Pacific, Geological Association of Canada, Mineralogical Association of Canada (GAC/MAC); joint annual meeting, Program with abstracts, v. 28. 2003-03 Copper, P. and Scotese, C.R., 2003. Megareefs in Mid-Devonian supergreenhouse climates.  In, M.A. Chan & A.W. Archer (eds.), Extreme depositional environments: mega end members in geologic time, Geological Society America Special Paper 370: 209-230, (93) Abstract: A newly refined reef database, modified to calculate reef tracts in relation to major tectonic plates, and with new paleogeographic maps, indicates that the largest known, and latitudinally most widespread Phanerozoic reefs developed during the Middle Paleozoic (Siluro-Devonian), with an acme in the Middle Devonian. Expanding during times of exceptional sea-level highstands and widespread epicontinental shallow seas, this 26 m.y. long acme of coral-sponge reef growth coincided with the warmest global temperatures known for the Phanerozoic, i.e., with a "supergreenhouse" climate mode well above Holocene interglacial norms. During the Middle Paleozoic, reefs were particularly abundant, occupying large, continental seaboard, carbonate platforms, and vast inland epicontinental seas. Examples of such "extremes" occurred mostly on passive margin settings, and extensive flooded continental interiors, e.g., the 1700-3000 km long tracts of the Western Canada Sedimentary Basin, Canadian arctic (Innuitian platform), eastern Laurentia "Old Red Continent" (United Kingdom to Poland), eastern Russian Platform (northeast Laurentia), Ural "Fold Belt" (eastern slopes of Urals), Siberia, northwest Africa, and South China. Smaller scale reef belts between 700 and 1300 km long were constructed on isolated tectonic terranes facing Gondwana on the north (Pyrenees, Afghanistan-Pakistan), Mongolia, Kolyma-Chukot, and North China. Large basins and flooded shelf areas, and the reefs featured within them, were not persistently developed throughout the Middle Paleozoic. They especially characterized the middle Emsian through Givetian (late Early Devonian-Middle Devonian). The following Frasnian (Late Devonian) showed more restricted and confined distribution of coral-stromatoporoid reefs, and during the Famennian, coral-stromatoporoid reefs "crashed" and were replaced by calcimicrobial reefs and platforms. During the latter phases of the Frasnian/Famennian mass extinctions, such microbial reefs were confined to relatively small areas, and metazoan reefs were nearly entirely obliterated, being confined to rare stromatoporoid patch reefs or lithistid mounds. Coral reefs were completely absent during the 21 m.y. long Famennian interval, and no real recovery of "keystone" frame-building, colonial corals took place in reef settings. The Famennian coincided with repeated glaciations, sharp sea-surface cooling events, sea-level drawdowns, and concurrent, matching stable isotope excursions. 2003-04 Scotese, C.R., 2003. Cretaceous and Cenozoic paleogeographic maps on pp. 15, 21, and 31, in Rick Gore, The Rise of Mammals: Adapting, Evolving, Surviving, National Geographic Magazine, April, 2003, vol. 203, number 4, p. 3-33, National Geographic Society, Washington, D.C. no abs 2003-05 Nokleberg, W. J., Bundtzen, T. K., Eremin, R.A., Ratkin, V.V., Dawson, K.M., Shpikerman, V.I., Goryachev, N.A., Byalobzhesky, S.G., Frolov, Y.F., Khanchuk, A.I., Koch, R.D., Monger, J.H.W., Pozdeev A.I., Rozenblum, I.S., Rodionov, S.M., Parfenov, L.M., Scotese, C.R., Sidorov, A.A., 2003. Metallogenesis and tectonics of the Russian Far East, Alaska, and the Canadian Cordillera, U.S. Geological Survey Open File Report 03-0434. 2003-06 Nokleberg, W.J., Monger, J.W.H., Scotese, C.R., Parfenov, L.M., Khanchuk, A.I., and Stone, D.B., 2003. Tectonic connections across the Circum-North Pacific: Constraints for paleogeography, Geological Association of Canada, Mineralogical Association of Canada; joint annual meeting, Program with abstracts, v. 28. 2003-07 Scotese, C.R., 2003. Permo-Carboniferous paleogeographic and paleoclimatic reconstructions, XVth International Congress on Carboniferous and Permian Stratigraphy, Utrecht, Netherlands, August 10-16, 2003, (abstract only). Plate tectonic, paleogeographic and paleoceanographic events during the Late Paleozoic may have transformed the Earth from a Hot House to Ice House world. In order to better understand the changing world of the Late Paleozoic, six, 3D paleogeographic models were built that illustrate the paleotopography of the continents and a speculative paleobathymetry of the Late Paleozoic ocean basins. 3D paleoglobes have been made for the latest Devonian (360 Ma), Mississippian (340 Ma), early Pennsylvanian (320 Ma), late Pennsylvanian, (300 Ma), and early Permian (280 Ma), and late Permian (260 ma). During the latest Devonian, a pre-Pangea had begun to assemble in the southern hemisphere. North America was in collision with northern South America, and the ocean basins between Europe and North Africa had nearly disappeared. Paleotethyan ocean basins, however, still separated Siberia from the Kazakhstan island arcs, and a wide ocean lay between the Cathaysian continents (N. & S. China) northern hemisphere continents. During the Mississippian, pre-Pangea rotated northward. The Canadian Arctic moved from an equatorial position to a subtropical latitude. The still emergent Caledonian and Northern Appalachians moved into the equatorial rainy belt. Siberia and the island arcs of Kazakhstan had begun to coalesce, and the Cathaysian continents (North and South China), now separate from Gondwana, were in transit across PaleoTethys. By the early Pennsylvanian western Pangea had assembled. The rising, equatorial, Central Pangean Mountains separated North America and Europe from the Gondwana continents. Kazakhstania and Siberia were in collision with Baltica. North China and South China were beginning to collide along the Tien Shan range of southern Kazakhstania. Through the late Pennsylvanian and earliest Permian, convergence and mountain building continued the consolidation of western Pangea. The paleotopography and paleobathymetry of the Late Paleozoic world has been modeled using 3D rendering software (Lightwave 3D 7.5). These 3D elevation models have a vertical resolution of 40 meters, and geographic resolution of approximately 10 km. 2003-08 Hyde, W.T., Grossman, E.L., Pollard, D., Scotese, C.R., Crowley, T .J., 2003. An Ice-Free Siberia: A Clue to Carboniferous CO2 Levels, American Geophysical Union 2003 Fall meeting, EOS, Transactions of the American Geophysical Union, v. 84, issue 46, Abstract PP21B-1174. 2003-09 Grossman, E.L., Hyde, W.T., Pollard, D., Scotese, C.R., 2003. Isotopic and Climate Model Constraints on Paleo-CO2 in the Late Paleozoic, American Geophysical 2003 Fall meeting, EOS, Transactions of the American Geophysical Union, v. 84, issue 46, Abstract PP21B-1175. 2003-10 Scotese, C.R., 2003. Paleogeographic Constraints on Biogeograpy: A New Set of Paleomaps, Symposium III: Paleobiogeography, Conveners, Julio Betancourt and Rob Hengeveld, Frontiers of Biogeography, Program and Abstracts, International Biogeography Society Inaugural Meeting, January 4-8, Oasis Resort, Mesquite, NV. Paleogeographic maps provide the spatial context for understanding, interpreting, and analyzing biogeographic patterns. A paleogeographic map, itself, is highly interpretive. On a global scale, a paleogeographic map must first illustrate the past positions of the continents and oceans according to the evidence from plate tectonics and paleomagnetism. However, this alone does not make a paleogeographic map. Once the global plate tectonic framework has been established, a paleogeographic map must describe the ancient distribution of highlands, lowlands, shallow seas and deep ocean basins. This is done by reconstructing the changes in topography and bathymetry caused by tectonic and erosional processes. Young tectonic features such as recent uplifts or volcanic eruptions must be removed or reduced in size, whereas older tectonic features such as ancient mountain ranges, must be restored to their former extent As an example the ocean floor which subsides as it cods and moves away from the mid-ocean ridge must be “revived” in order to bring it back to its former depths. Once the ancient topography and bathymetry has been recreated, it is then possible to begin understand the gateways and barriers that control biogeographic pathways.At the turn of the Twentieth Century, the unsuccessful attempts to explain ancient biogeographic patterns using modern geography were, in part, responsible for the formulation and acceptance of continental drift. At the turn of the Twenty-first Century, were are now poised to apply advances in plate tectonics and,, paleoclimatic and paleoceanographic modeling, to produce new set of detailed paleogeographic maps that can be used to unravel the complex pattern of Phanerozoic biogeographic change. In this presentation a set of 3D “paleo-globes” will be presented for the Cenozoic, Mesozoic, and late Paleozoic. 2003-11 Scotese, C.R., The World according to Chris Scotese: The PALEOMAP Project Maps the Past, Present and Future, Dallas Geological Society, April 16, 2003, Dallas, Texas. The PALEOMAP Project is known for its synthesis of the plate tectonic, paleogeographic, and paleoclimatic history of ocean basins and continents during the last 1100 million years, and the illustration of Earth history through maps, computer animations, and Geographic Information Systems (GIS). In this talk, Chris will present his latest 3D paleogeographic and plate tectonic maps and animations. Global plate tectonic, paleogeographic and paleoclimatic reconstructions will be presented for the last 200 million years. These reconstructions use 3D paleotopographic and paleobathymetric information to represent the surface of the Earth and the shape and depth of the ocean basins. Each map is composed of over 6 million pixel-points that capture digital elevation information at a 10 x 10 km geographic resolution and 40 meter vertical resolution. This quantitative, digital approach to paleogeographic modeling permits new ways to visualize and analyze the changing surface of the Earth through time using standard GIS (ESRI 3D Analyst, Spatial Analyst), 3D modeling, and computer animation techniques. The process of building a 3D paleogeographic map begins with the digital topography and bathymetry compiled by NOAA (Smith & Sandwell, 2001), the BEDMAP Project (British Antarctic Survey), and the IBCAO Arctic Project (Jakobsson et ah, 2000). The topographic and bathymetric information is gridded at a 6-minute resolution, and the individual data points (pixel-points) are rotated back to their paleopositions using the global plate tectonic model of the PALEOMAP Project. The resulting map is reconstruction of present-day bathymetry and topography in paleo-coordinates (Early Cretaceous, Figure 1 ) In the next processing steps, the digital elevation and bathymetric values are corrected to take into account the complex effects of thermal subsidence (Stein & Stein, 1992), glacial rebound, tectonic and volcanic activity and erosion. The result is a revised, global paleotopographic and paleobathymetric surface. To complete the 3D paleogeographic model, the new topographic surface is digitally “flooded” by raising or lowering sea level according to the estimates from eustatic sea level curves (e.g., Haq et al., 1987). This new paleogeographic mapping technique raises interesting geological questions. For instance, the shorelines shown in the early Miocene map (Figure 2 ) are familiar but not identical to today’s coastlines. Florida is flooded, as are the molasse basin of the Alps, Persian Gulf foredeep and the peri-Caspian region. But surprisingly, so are the Amazon and Parana basins. Conversely, if sea level were higher, one might expect that Southeast Asia would be flooded. However, geologic evidence indicates that Southeast Asia was emergent during the early Miocene. This suggests that dynamic plate tectonic forces associated with subduction in the Java-Sumatra trench may be “pulling-down” the leading edge of Indonesia. The digital topographic and bathymetric models presented here are currently being used for paleoclimatic and paleoceanographic simulations. They provide the framework and foundation for a detailed and quantitative modeling of Earth surface processes since the late Precambrian. 2003-12 Scotese, C.R. AMZ Retirement Meeting 2003-13 A&M meeting no abs First Edition of PaleoAtlas for ArcGIS 2004 Milestones: 1) Pgeog Video on DVD, St. Louis, 2) Erlanger Meeting, 3) Lille, 4) Flip book J. Geology, 5) Paleogeography Dercourt Meeting, Paris, France 2004-01 Krause, F. F., Scotese, C.R., Nieto, C., Sayegh, S.G., Hopkins, J.C. and Meyer, R.O., 2004. Paleozoic stromatactis and zebra carbonate mounds: Global abundance and paleogeographic distribution, Geology, v. 32, no. 3, 181-184.(97) Abstract (English): Carbonate mud-mounds with zebra and stromatactis structures are present in every Paleozoic system and series, but are more common in Devonian and Carboniferous deposits, reaching their acme in Mississippian System (lower Carboniferous) rocks. Global distributions illustrate that mud-mounds spanned the planet ranging from tropical to polar circles. Such a wide latitudinal span signifies that they not only grew in and occupied warm depositional environments, but also in settings where oceanic waters were cold and seasonally light limited. Moreover, their proliferation during the Devonian and Carboniferous was at a time when planet-wide climatic ice-house conditions are thought to have prevailed. Mud-mounds, therefore, may also be products of cool and cold-water carbonate sedimentation. 2004-02 Scotese, C.R., 2004, Cenozoic and Mesozoic Paleogeography: Changing Terrestrial Biogeographic Pathways, in Frontiers of Biogeography: New Directions in the Geography of Nature, M.V. Lomolino and L.R. Heaney, (editors), Sinauer Associates, Inc., Sunderland, Massachusetts, p. 1-26. (96) 18 plate tectonic and paleogeographic maps illustrate the changing configuration of continents and ocean basins during the last 240 million years. Terrestrial biogeographic pathways have been primarily controlled by the breakup of the early Mesozoic supercontinent, Pangea, and the global rise and fall of sea level. Pangea, which was intact during the Triassic and early Jurassic, greatly facilitated inter-continental terrestrial migration (the Pangean Superhighway). The progressive breakup of Pangea during the Late Jurasssic and Cretaceous resulted in the piecemeal isolation of the fauna and flora of the major continents. However, these long-term plate tectonic effects (millions of years) were complicated by short-term (100,000's of year) changes in sea level. The rise and fall of sea level opened and closed terrestrial gateways between the continents. Some of the most important gateways were the: Panamanian Isthmus, the New Guinea-Timor-Sumba collision zone,, the Bering Sea land bridge, the Svalbard and the Faroes-Iceland corridors, isolation of India and its subsequent collision with Asia, and the complex sequence of changing Cretaceous connections between the Gondwana continents (South America-Africa-Madagascar-India-Australia and Antarctica). 2004-03 Scotese, C. R., Parfenov, L. M., Khanchuk, A. I., Berzin, N. A., Badarch, G., Tomurtogoo, O., Kuzmin, M. I., Yan, H., and Nokleberg, W. J. 2004. Dynamic computer model for the tectonics of Northeast Asia, IAGOD Interim Conference, Far Eastern Geological Institute, 151 pp. A dynamic model for the Proterozoic and Phanerozoic tectonic development of the Northeast Asia (Eastern and Southern Siberia, Mongolia, Northeastern China, South Korea, Japan, and adjacent offshore areas) is illustrated in a computer movie that displays the successive formation of major regional geologic units from the Paleoproterozoic through the Present. The tectonic development of the region is recorded in the cratons, craton margins, oceanic plates, active rifts, and orogenic collages of the Northeast Asia continent and eastern active continental margin. The collages consist of tectonostratigraphic terranes that are composed of fragments of igneous arcs, accretionary-wedge and subduction-zone complexes, passive continental margins, and cratons. The tectonostratigraphic terranes are overlapped by continental-margin-arc and sedimentary-basin assemblages. The tectonic history of cratons, craton margins, oceanic plates, terranes, and overlap assemblages is complex due to extensional dispersion and translation during strike-slip faulting that occurred subparallel to continental margins. The dynamic tectonic model portrays the major geologic events that formed this large region. The major events are: (1) major periods of rifting in the Neoproterozoic, Late Devonian, and Early Carboniferous that occurred along the ancestral margins of present-day Northeast Asia. (2) From about the Devonian through the mid- Cretaceous, a succession of island arcs and tectonically paired subduction zones that formed mainly near continental margins. (3) From about mainly the mid-Cretaceous through the Present, a succession of igneous arcs and tectonically paired subduction zones that formed along the continental margin. (4) From about the Jurassic to the Present, oblique convergence and rotations that caused orogen-parallel sinistral, and then dextral displacements within the upper plate margin of cratons that have become Northeast Asia. (5) From the Early Jurassic through Tertiary, movement of the upper continental plates toward subduction zones that resulted in strong plate coupling and accretion of the former island arcs, subduction zones to continental margins. Accretions were accompanied and followed by crustal thickening, anatexis, regional metamorphism, and uplift. (6) In the middle and late Cenozoic, oblique to orthogonal convergence of the Pacific Plate with present-day Alaska and Northeast Asia resulted in formation of the modern-day ring of volcanoes along the eastern margin of the Northeast Asia. 2004-04 Boucot, A.J., Xu, Chen, and Scotese, C.R., 2004. Phanerozoic Climatic Zones and Paleogeography with a Consideration of Atmospheric CO2 Levels, Paleontological Journal, v.38, issue 2, p. 115-122. just abs? 2004-05 Scotese, C.R., 2004. Early Paleozoic Plate Tectonics, Paleogeography and Paleoclimate, International Sympsium on Early Paleozoic Paleogeography and Paleoclimate, September 1-3, Erlangen, Germany, Erlanger Geologische Abhandlungen, Sonderband 5, p. 64. Ten paleoreconstructions are presented illustrating the plate tectonics, paleogeography and paleoclimate of the latest Precambrian and Early Paleozoic. The time intervals chosen include two maps for the latest Precambrian (600 Ma and 570 Ma), maps for the Early and Late Cambrian, four maps for the Ordovician (early Tremadoc, early Arenig, Llandeilo/Caradoc, and Ashgill), as well as paleoreconstructions for the Early and Middle Silurian. The plate tectonic reconstructions show the probable location of active plate boundaries (subduction zones, island arcs and mid-ocean ridges). The paleogeographic maps illustrate the distribution of deep oceans, shallow shelves, lowlands and mountainous areas for each time interval. There are two versions of each paleogeographic map. One map shows the extent of maximum flooding during a period of high eustatic sea level. The second map shows the paleogeography during a time of minimum sea level corresponding to a major sequence boundary. In the final set of maps, climatically sensitive lithofacies such as evaporites, calcretes, bauxites, and tillites are plotted on the paleoreconstructions. Climatic zones are mapped based on the distribution of these climatically sensitive lithofacies. also ppt 2004-06 Scotese, C.R., 2004. Early Paleozoic Paleoclimate Simulations: Data and Model Comparisons, International Symposium on Early Paleozoic Paleogeography and Paleoclimate, September 1-3, Erlangen, Germany, Erlanger Geologische Abhandlungen, Sonderband 5, p. 65. Computer models that are used to simulate paleoclimate, such as GCMs and FOAMs are expensive to run, use excessive amounts of computing time, and often give results that are in poor agreement with the geological record. GCMs are notorious for results that look more like the present-day than the geological past. Hot Houses climates, like the Cretaceous, have been especially difficult to simulate. Though the GCM simulations for Hot House climates can be improved by drastically increasing CO2, levels or enhancing equator-to-pole oceanic transport, these adjustments often seem forced and ad-hoc. An alternate climate modeling technique has been developed by the author, called the Parametric Climate Model (PCM), that is inexpensive, can be run quickly on personal computers, and makes paleoclimatic predictions that are in better agreement with the rock record. The PCM is a non-dynamical climate model uses geological information describing past climates to set important boundary conditions for the paleoclimatic simulations. These boundary conditions include: the pole-to-equator temperature gradient, surface moisture, land cover, and the size and extent of the paleo-Hadley cell circulation. Most of the computing time and expense of a GCM run is the result of the repetitive calculations required to “spin up” a dynamical simulation of the oceans and atmosphere. Only after running for a number of “model years” (often weeks of computing time) are the estimates considered accurate. In contrast, the PCM starts with boundary conditions that reflect our knowledge of past climates and consequently gives more geologically satisfying results. To test the Parametric Climate Model, five paleoclimatic simulations were run for the: Late Precambrian (600 Ma), the Early Cambrian, the Early Ordovician, the latest Ordovician (Ashgill), and the Middle Silurian (Wenlock). Global temperatures, precipitation patterns, surface ocean currents and upwelling zones that were predicted by the PCM were compared with available GCM runs and with the distribution of lithologic indicators of climate such as evaporites, calcretes, bauxites, kaolinites, and tillites. A database of lithologic indicators of climate comprising more than 8000 entries for the Phanerozoic has been compiled by A.J. Boucot (Oregon) and Chen Xu (Nanjing). also poster 2004-07 Boucot, A.J., Xu, Chen, and Scotese, C.R., 2004. Phanerozoic Climatic Zones and Paleogeography with a Consideration of Atmospheric CO2 Levels, in Journal of Paleotopography (Russian), No. 2, p. 3-11. (98a) Abstract: Compilation of climatically sensitive deposits (chiefly evaporites, calcretes, coals, bauxites, kaolin’s and kaolinites, tillites, dropstones, glendonites and cool-water marine sediments, palms, as well as crocodilians etc.) through twenty-seven Phanerozoic time intervals enables one to revise the contemporary paleogeography in a manner consistent with the climatic information. We also take account of some of the available biogeographic information. Comparison of the changing Phanerozoic global climatic gradients based on geological evidence with the previously published models of Phanerozoic atmospheric CO (sub 2) based on geochemical assumptions indicates that either the assumptions on which the geochemical models are based are erroneous or that atmospheric CO (sub 2) is not a greenhouse gas. We prefer the former possibility. 2004-08 Scotese, C.R., 2004. A continental drift flipbook, Journal of Geology, v. 112, issue 6, p. 729-741. (95) Abstract: Forty-six miniature plate tectonic reconstructions are presented that can be assembled into a "flipbook" that illustrates the movement of the continents since the Late Precambrian, 750 m.yr. ago. Six principal lines of evidence have been used to reconstruct the past positions of the continents: (1) linear magnetic anomalies produced by sea floor spreading, (2) paleomagnetism, (3) hotspot tracks and large igneous provinces, (4) the tectonic fabric of the ocean floor mapped by satellite altimetry, (5) lithologic indicators of climate (e.g., coals, salt deposits, tillites), and (6) the geologic record of plate tectonic history. I discuss the probable uncertainties associated with the plate tectonic reconstructions and give an estimate of the uncertainty in the positions of the continents back through time. 2004-09 Krause, F. F., Scotese, C.R., Nieto, C., Sayegh, S.G., Hopkins, J.C. and Meyer, R.O., 2004. Paleozoic carbonate mud-mounds: Global abundance and paleogeographic distribution, AAPG 2004 Annual Meeting, Annual Meeting Expanded Abstracts - American Association of Petroleum Geologists, volume 13, p. 78. Abstract: Carbonate mud-mounds with zebra and stromatactis structures are present in every Paleozoic system and series. Yet within this interval they are more common in middle and lower upper Paleozoic deposits, reaching their abundance acme in Lower Carboniferous Series rocks. In addition, global paleogeographic distribution plots of mud-mounds illustrate that they spanned the globe during the Paleozoic, as they are found at localities that were positioned from tropical to polar circles. That these carbonate buildups covered such a wide latitudinal span signifies that they were not limited to tropical marine settings, but that they grew and occupied a wider ecosedimentary spectrum that included locales where oceanic waters were cold and seasonally light-limited. Moreover, the proliferation of mud-mounds during the middle and lower upper Paleozoic is curious in that it parallels a period during which global climatic ice-house conditions are thought to have prevailed on the planet. Thus, mud-mounds may be products of cool and cold-water carbonate sedimentation and should be reexamined and studied with this alternative in mind. 2004-10 Scotese, C.R., 2004. 3D Paleogeographic Maps and Animations for the Mesozoic and Cenozoic, 51st Annual Systematics Symposium,"Latin American Biogeography - Causes and Effects", Missouri Botanical Garden, October 8-10, 2004, Abstracts with Program, p X. 2004-11 Scotese, C.R and Rees, P. Mc., 2004. The Spatial-Temporal Information Matrix (STIM cube): An Efficient Way to Store Geological Information, Geological Society of America 2004 Annual Meeting, Denver CO., Abstracts with Programs, v. 36, issue 5, p. 153. Abstract: Geologists have traditionally used maps and stratigraphic sections to describe the spatial and temporal location of geological information. The "Spatial-Temporal Information Matrix", or STIM is the digital equivalent of these tools. A hyperdimensional cube, the STIM model permits the storage and quick retrieval of all kinds of geological information. The three principal axes of the STIM model can be visualized as a cube whose Z-axis is time, and whose X &Y axes are present-day geographic coordinates (latitude and longitude). The STIM cube can be subdivided into billions of "box-cells", or boxels. Each boxel can hold any type of geological information. It can be a "value" (e.g. paleo-elevation, rock property, or geochemical measurement) or an "index" that points to values or attributes in a more complex table or database. Some of the advantages of STIM are: 1) it is compatible with existing geographic information systems (GIS), 2) it permits data from many different data sources to be combined in a common data structure, 3) it allows new associations to be made between disparate data types, 4) and it provides a new way to visualize spatial-temporal data . Inexpensive mass-storage makes the STIM model physically possible. It is estimated that a STIM model describing the geophysics, geochemistry, and stratigraphy of the Earth back to the late Precambrian would require approximately 50 terabytes. Further efficiencies and increases in resolution could be made by implementing a method of dynamic scaling that modifies the size of each boxel depending on the data density and resolution. To test the STIM approach the authors are constructing a STIM cube that describes the paleo-position of any present-day geographic feature back through time. In this data model, the uppermost level of the cube is an x-y grid of present-day latitude and longitude. Each boxel (specified by latitude, longitude and time) contains the paleo-latitude and paleo-longitude of that geographic location back through time. This Paleo-Reconstruction Information Matrix (PRIM) would allow users to produce paleo-reconstructions illustrating the past locations of any kind of geological data set. A PRIM cube with a boxel size of one degree by one degree, and a temporal resolution of 1 million years would require only 80 megabytes of storage. 2004-12 Kominz, M.A., and Scotese, C.R., 2004. Plate reconstructions require high Cretaceous spreading rates and ridge volumes, Geological Society of America 2004 Annual Meeting, Denver, CO, Abstracts with Programs, v. 36, issue 5, p. 259. Abstract: High Cretaceous seafloor spreading rates have been implicated in the production of CO (sub 2) and thus, the greenhouse climate as well as in the generation of high eustatic sea level. The sources of data on which spreading rates are based are spreading plate models that are based, in turn, on magnetic anomalies and the time scales used to date them. Both have been refined over the past 20 years since the last ridge volume calculations were made and both retain some uncertainty. Subduction of seafloor necessarily reduces the accuracy of estimates of past ocean volumes at increasingly older times. However, the Atlantic and Indian Oceans (AIO) provide a relatively complete record of spreading rates for the past 170 Ma, because subduction is minor in these basins. The volume of the AIO ridges grew through time to about 50 Ma as plates systematically fragmented Gondwana. The subsequent contribution of oceanic area from AIO oceans remained generally high with variations that depend on the time scale applied to magnetic anomalies. The area of the Pacific Ocean is slightly larger than the Atlantic and Indian Oceans combined and, thus, was probably nearly twice its current size in the Early Cretaceous. Here seafloor from the N, E and SE sides of the late Cretaceous Pacific Plate have been subducted along with all or most of the Farallon-Phoenix and the Kula-Phoenix Ridges. The spreading rates of these ridges can be inferred from the remaining triple junctions on the western half of the Pacific Plate. The lengths of these ridges depend on the plate reconstruction chosen. A reconstruction at 90 Ma allows examination of spreading rates and the age distribution at this time. Spreading rates were very high and in the absence of slow spreading AIO ridges, require significantly higher spreading rates compared to those of the last 50 Ma. This is reflected in the area-age distribution of sea floor, which reflects the younger nature of ocean floor compared to the area-age distribution observed today. 2004-13 Schillig, P.C., Scotese, C.R., Coshell, L., and Gierlowski-Kordesch, E., 2004. Lake distribution in the Eocene, Geological Society of America Annual Meeting, Denver, CO, Abstracts with Programs, v. 36, issue 5, p 34. Abstract: Besides oceans, lakes can have a profound influence on climate patterns through atmosphere-water feedbacks via the "lake effect". They serve as heat sinks and moisture sources that can affect intracontinental climates, as demonstrated by the Permian lakes in southern Gondwanaland or even the Great Lakes in North America. Lake distribution data from the geologic past will have considerable potential for testing and refining reconstructions of atmospheric paleocirculation as well as producing more accurate paleogeographic maps. According to both marine and terrestrial data, Eocene climate has been documented as the warmest period of the Cenozoic. In Eocene age sequences, lake deposits are associated with rift and thrust zones that are spread across North America, southeast Asia, Australia, and western Europe. The interrelationship between tectonics and the formation of lakes is well established; however, the reasons for the thermal maximum during the Eocene are still under debate. Proposed warming mechanisms include injection of metamorphic thermogenic and wetland methane, release of organically-derived carbon dioxide, poleward oceanic heat transfer, and reduction in the intensity of atmospheric circulation. Heat retention and transfer are important in all these mechanisms. Did the large number of lakes in the Eocene, as evidenced by their preserved deposits, add a "lake effect" to the high global temperatures? To address the lake effect problem in the Eocene, a paleogeographic map of lake distribution must first be generated. Data for approximately one hundred Eocene lake deposits were compiled through a literature search and use of the GGLAB database (Global Geological Record of Lake Basins). Information such as present location, relative age, and projected areal deposit extent (km2) were recorded along with citations. Time resolution of the lake deposits were separated out at the scale of the lower, middle, and upper Eocene. Compiled data was plotted on Eocene maps of the PALEOMAP Project. Analysis of lake extent and distribution through the Eocene will follow. 2004-14 Scotese, C.R., 2004. Early Paleozoic Plate Tectonics, Paleogeography and Paleoclimate, 48th Paleontological Association Annual Meeting, Lille, France, December, 17-24, 2004, Abstracts with Programme, v. 36, issue 5, p. 109. Ten paleoreconstructions are presented, illustrating the plate tectonics, paleogeography and paleoclimate of the Latest Precambrian and Early Paleozoic. The time intervals chosen include two maps for the latest Precambrian (600 Ma and 570 Ma), maps for the Early and Late Cambrian, four maps for the Ordovician (early Tremadoc, early Arenig, Llandeilo/Caradoc, and Ashgill), as well as paleoreconstructions for the Early and Middle Silurian. The plate tectonic reconstructions show the probable location of active plate boundaries (subduction zones, island arcs and mid-ocean ridges). The paleogeographic maps illustrate the distribution of deep oceans, shallow shelves, lowlands and mountainous areas for each time interval. There are two versions of each paleogeographic map. One map shows the extent of maximum flooding during a period of high eustatic sea level. The second map shows the paleogeography during a time of minimum sea level corresponding to a major sequence boundary. In the final set of maps, climatically sensitive lithofacies such as evaporites, calcretes, bauxites, and tillites are plotted on the paleoreconstructions. Climatic zones are mapped based on the distribution of these climatically sensitive lithofacies. 2004-15 Scotese, C.R., 2004. 3D Paleogeography and Computer Animations of Earth History, in Colloque de Paleogeographie, 8 et 9 Mars, 2004, Institut de France - Academie des sciences, 23, quai de Conti, 75006, Paris, Resumes. The PALEOMAP Project is known for its synthesis of the plate tectonic, paleogeographic, and paleoclimatic history of ocean basins and continents during the last 1100 million years. In this talk, Prof. Scotese will present his latest 3D paleogeographic and plate tectonic maps and animations for the Late Precambrian, Paleozoic, Mesozoic and Cenozoic. These reconstructions use 3D paleotopographic and paleobathymetric information to represent the surface of the Earth and the shape and depth of the ocean basins. Each map is composed of over 6 million "pixel-points" that capture digital elevation information at a 10 x 10 km geographic resolution and 40 meter vertical resolution. This quantitative, digital approach to paleogeographic modeling permits new ways to visualize and analyze the changing surface of the Earth through time using Geographic Information Systems, 3D modeling, and computer animation techniques. The process of building a 3D paleogeographic map begins with the digital topography and bathymetry compiled by NOAA (Smith & Sandwell, 2001), the BEDMAP Project (British Antarctic Survey), and the IBCAO Arctic Project (Jakobsson et al., 2000). The topographic and bathymetric information is gridded at a 6-minute resolution, and the individual data points (pixel-points) are rotated back to their paleopositions using the global plate tectonic model of the PALEOMAP Project. The resulting map is reconstruction of present-day bathymetry and topography in paleo- coordinates (Early Cretaceous, Figure 1 ). In the next processing steps, the digital elevation and bathymetric values are corrected to take into account the complex effects of thermal subsidence (Stein & Stein, 1992), glacial rebound, tectonic and volcanic activity and erosion. The result is a revised, global paleotopographic and paleobathymetric surface. To complete the 3D paleogeographic model, the new topographic surface is digitally “flooded” by raising or lowering sea level according to the estimates from eustatic sea level curves (e.g., Haq et al., 1989). The digital topographic and bathymetric models presented here are currently being used for paleoclimatic and paleoceanographic simulations. They provide the framework and foundation for a detailed and quantitative modeling of Earth surface processes since the late Precambrian. 2005 Milestones: Begin GANDOLPH Project, McKerrow Symposium 2005-01 Main, D., and Scotese, C.R., 2005. Cretaceous paleogeography and the paleobiogeographic dispersal of the hadrosaurs, Poster Session B, Abstracts of Papers, Sixty-fifth annual meeting, Society of Vertebrate Paleontologists, Mesa Southwest Museum and Phoenix Marriott Mesa, Mesa, Arizona, October 19-22, 2005, Journal of Vertebrate Paleontology, v. 25, issue 3, p. 88. 2005-02 Nokleberg, W. J., Parfenov, L. M., Khanchuk, A. I., Bardach, G., Ogasawara, M., Hwang Duk-Hwan, Yan Hongquan, and Scotese, C. R, 2005. Major products of the international collaborative project on mineral resources, metallogenesis, and tectonics of northeast Asia, Proceedings of the 8th Biennial SGA (Society for Geology Applied to Mineral Deposits) Meeting, v.2, p. 1157. 2005-03 Schettino, A., and Scotese, C.R., 2005. Apparent polar wander paths for the major continents (200 Ma to the present day): A paleomagnetic reference frame for global plate tectonic reconstructions, Geophysical Journal International, v. 163, issue 2, 727-759. (99a) Abstract: Synthetic apparent polar wander (APW) paths for North America, South America, Eurasia, India, Central Africa, Australia and Antarctica for the last 200 Myr are proposed. Computation of these APW paths is based upon the latest version (4.5a) of the Global Paleomagnetic Database (GPMDB), a revised global plate tectonic model since the Early Jurassic, and a new technique for generating smoothed APW paths. The smoothing technique includes the following steps: (1) pre-selection of palaeopoles, including pre-filtering parameters (number of sites, number of samples per site, 95 per cent confidence circle about mean direction, cleaning procedure, and time uncertainty); (2) generation of palaeolatitude and declination plots for a reference site on each continent that combines palaeopoles via a global plate tectonic circuit; (3) independent spline regression analyses of the palaeolatitude and declination plots; (4) removal of palaeolatitude or declination data that deviate by more than 10° from the regression curves (post-filtering process); (5) generation of synthetic APW paths from the resulting palaeolatitude and declination plots. These synthetic APW paths are then rotated into African coordinates to determine the best-fit APW path and a global palaeomagnetic reference frame. Four representative plate tectonic reconstructions and global plate velocity fields are presented for the three time intervals that correspond to globally synchronous changes in plate motion. 2005-04 Nokleberg, W. J., Bundtzen, T. K., Eremin, R. A., Ratkin, V. V., Dawson, K. M., Shpikerman, V. I., Goryachev, N. A., Byalobzhesky, S. G., Frolov, Yu. F., Khanchuk, A. I., Koch, R. D., Monger, J. W. H., Pozdeev, A. I;., Rozenblum, I. S., Rodionov, S. M., Parfenov, L. M.,; Scotese, C. R., Sidorov, A. A., 2005. Metallogenesis and tectonics of the Russian Far East, Alaska, and the Canadian Cordillera, U.S. Geological Survey Professional Paper 1697, 397 pp. (99c) Abstract: The Proterozoic and Phanerozoic metallogenic and tectonic evolution of the Russian Far East, Alaska, and the Canadian Cordillera is recorded in the cratons, craton margins, and orogenic collages of the Circum- North Pacific mountain belts that separate the North Pacific from the eastern North Asian and western North American Cratons. The collages consist of tectonostratigraphic terranes and contained metallogenic belts, which are composed of fragments of igneous arcs, accretionary-wedge and subduction-zone complexes, passive continental margins, and cratons. The terranes are overlapped by continental-margin-arc and sedimentary-basin assemblages and contained metallogenic belts. The metallogenic and geologic history of terranes, overlap assemblages, cratons, and craton margins has been complicated by postaccretion dismemberment and translation during strike-slip faulting that occurred subparallel to continental margins. 2005-05 Main, D., and Scotese, C.R., 2005. Polar paleogeographic maps: a framework for Mesozoic dinosaur biogeographic pathways, North American Paleontology Convention (NAPC), PaleoBios, v.25, Issue, p. 79. 2005-06 Scotese, C. R., Nokleberg, W. J., Parfenov, L. M., Bardach, G., Berzin, N. A., Khanchuk, A. I., Kuzmin, M. I., Obolenskiy, A. A;., Prokopiev, A. V., Rodionov, S. M., Yan Hongquan, 2005. Tectonic and metallogenic evolution of northeast Asia; key to regional understanding, Proceedings of the 8th Biennial SGA (Society for Geology Applied to Mineral Deposits) Meeting, v.2, p. 1183-1184. 2005-07 Zumberge, J.E., Scotese, C.R., Brown, S.W., and Illich, H.A., 2005. Crude oil predictions of source rock depositional environments help constrain paleoclimatic models, 22nd IMOG. 2005-08 Scotese. C.R., 2005. Early Paleozoic plate tectonic, paleogeographic and paleoclimatic reconstructions: a W.S. McKerrow Legacy, W. S. McKerrow Memorial Symposium, Oxford University, Oxford England, January 15, 2005. Abstract: In 1973, I met Professor W. S. McKerrow from Oxford. Mac was visiting Fred Ziegler at the University of Chicago, and had come to the University of Illinois, where I was an undergraduate, to give a lecture in the Department of Geological Sciences. The topic of his lecture was tire new set of Phanerozoic reconstructions by Smith, Briden and Drewry (Smith et al., 1973). This chance meeting and the discussions that followed inspired me to make maps, “flip books” and computer animations illustrating the history of plate motions. The ten paleoreconstructions presented here illustrate the plate tectonics, paleogeography and paleoclimate of the Latest Precambrian and Early Paleozoic and are an update of the maps published in McKerrow and Scotese, 1990. The time intervals chosen include two maps for the latest Precambrian (600 Ma and 570 Ma), maps for the Early and Late Cambrian, four maps for the Ordovician (early Tremadoc, early Arenig, Llandeilo/Caradoc, and Ashgill), as well as paleoreconstructions for the Early and Middle Silurian. The plate tectonic reconstructions show the probable location of active plate boundaries (subduction zones, island arcs and mid-ocean ridges). The paleogeographic maps illustrate the distribution of deep oceans, shallow shelves, lowlands and mountainous areas for each time interval. There are two versions of each paleogeographic map. One map shows the extent of maximum flooding during a period of high eustatic sea level. The second map shows the paleogeography during a time of minimum sea level corresponding to a major sequence boundary. In the final set of maps, climatically sensitive lithofacies such as evaporites, calcretes, bauxites, and tillites are plotted on the paleoreconstructions. Climatic zones are mapped based on the distribution of these climatically sensitive lithofacies. 2005-09 Moore, T.L., Perlmutter, M.A., Scotese, C.R., 2005. Global and regional impacts of orbital cycles on the climate and sedimentation of icehouse and greenhouse worlds, Symposium on Greenhouse versus Icehouse: Genetic and Stratigraphic Differences, 2005 AAPG Annual Convention, June 19-22, 2005, Calgary, Canada, Abstracts: Annual Meeting - American Association of Petroleum Geologists v. 14, p. A94. Abstract: The Cenomanian/Turonian has been interpreted as a greenhouse world; a time with high atmospheric CO2 and no significant glaciation. In contrast, the Sakmarian has been interpreted as an icehouse world; a time with low atmospheric CO2 and major glaciation. These "end-member" conditions were not invariant. Milankovitch cycles produced climate changes throughout both these periods. To determine how climates varied, we used the Fast Ocean/Atmosphere Model (FOAM) at Argonne National Laboratory. Insolation extremes occur during periods of high eccentricity combined with the effects of precession, which can generate the highest summer and lowest winter insolation cases, and high obliquity, which can cause the greatest insolation contrast between summer and winter. To evaluate these effects on climate, simulations were run for each end member; one using a precession value placing the northern hemisphere closest to the sun in the summer, and one placing the northern hemisphere farthest from the sun in the summer. The model results showed: (1) interaction of eccentricity and precession is responsible for most climate variation; obliquity being responsible for far less change; (2) eccentricity and precession cause the northern and southern hemisphere climates to be out of phase; (3) within hemispheres, some regions demonstrate large climate changes while others remain stable; (4) climate changes related to Milankovitch cyclicity occur in both greenhouse and icehouse worlds; and (5) climate related processes such as weathering, erosion, sedimentation and deposition will be strongly affected by changes in orbital patterns, as well. 2005-10 Scotese, C.R., 2005. Africa: Paleogeography (200 million years to Present-day), 4th HGS/PESGB International Conference on Africa Exploration & Production, Houston, September 7-8, 2005, p. 15. Abstract: A computer animation is presented that illustrates the plate tectonic and paleogeographic development of Africa from the Early Jurassic (200 ma) to the present-day. The animation is based on 21 paleo-Digital Elevation Models (paleo-DEMs) that illustrate Africa's: ancient and active plate boundaries, paleotopography and paleobathymetry, and paleolatitudinal position through time. These paleo-DEMs are part of the Earth System History GIS (ESH-GIS), a digital geological atlas assembled by the PALEOMAP Project. Africa formed the core of the supercontinent of Pangea. The animation begins in the Early Jurassic, as flood basalts in South Africa and the sub-Saharan region heralded the breakup of Pangea. During the Middle and Late Jurassic rifting and sea floor spreading along Africa's east coast formed conjugate passive margins with northwestern India, western Madagascar and the Queen Maud Land sector of Antarctica. At the same time, North America separated from northwestern Africa forming the Central Atlantic Ocean. The next phase of rifting began in the earliest Cretaceous (Figure 1) as South America slowly pulled away from Africa, progressively forming the passive margin basins that stretched from the Guinea Plateau to the Cape of Good Hope. These basins formed earlier in the south (pre-Aptian) and later in the north (post-Aptian). Basin formation was accompanied by a complex phase of transtensional and transpressive deformation across central Africa. By the late Albian (-100 Ma), (Figure 2) all continental connections between Africa and the surrounding continents had been broken. During the early Cenozoic Africa continued its northward movement, and the northernmost fringes of the African plate (Apulian prong) began to collide with Europe, forming the Alps and Balkan mountain ranges. The collision of Arabia along the Zagros mountains began in the late Eocene. In the Oligocene, the East African Rift began to form as Somalia together with Arabia moved to the northeast. Arabia, bounded by the Red Sea and Gulf of Aden became a separate plate in the Miocene. 2005-11 Kominz, M.A., and Scotese, C.R., 2005. Thermal cooling of ocean lithosphere: New data new insights, American Geophysical Union 2005 Fall Meeting, San Francisco, CA, Eos, Transactions, American Geophysical Union, v. 86, issue 52, Abstract T23A-0537. 2005-12 Scotese, C. R., 2005. Frames from computer animation in, Kim Pewitt-Jones, Underground Movement, Research: The University of Texas at Arlington, Fall, 2005, p. 22 - 23, Arlington, TX. no abs 2005-13 Scotese, C.R., 2005. Plate tectonic history of the continental fragments comprising the Seychelles, Laxmi Ridge, Saya de Malha Bank and Nazareth Bank (for the Government of Mauritius, Indian Ocean). 2005-14 Scotese, C.R., 2005. Permian paleogeographic map, p. 64, in Virginia Morell, When Monster Ruled the Deep, National Geographic Magazine, volume 208, number 6, December 2005, p. 58-87. no abs 2005-15 (see 2005-10) 2005-16 Zumberge, J.E., Scotese, C.R., Brown, S.W., and Illich, H.A., Crude oil predictions of source rock depositional environments help constrain paleoclimatic models, 4th HGS/PESGB International Conference on Africa Exploration & Production, Houston, September 7-8, 2005, p. 29. Abstract: Marine shale, marl, carbonate and lacustrine source rock types of various geological ages can be predicted using terpane and sterane biomarkers in corresponding crude oils. Paleo-latitude and paleo-longitude locations of over 1800 crude oils comprising more than 130 known petroleum systems are calculated based on the present day oil location and the age of the corresponding source rock deposition. The oils can then be plotted on appropriate rotated plate reconstructions depicting paleo topography, bathometry, SST, prevailing wind directions, and areas of upwelling. When considering paleo latitudes, carbonate source rocks throughout the Phanerozoic were deposited within 25 degrees of the paleo-equator. Key tri- and tetracyclic terpane ratios potentially distinguish between warm, shallow intra-shelf source rock environments and cold, deeper-water upwelling areas of source rock deposition. 2005-17 CRS Rio de Janiero, Brazil meeting, no abs 2005-18 Scotese, C.R., 2005, The Earth in Flux, Plate 7, Evolution of the Earth, in Atlas of the World, 8th edition, National Geographic Society, Washington, D.C., 134 pp. 2006 Milestones: Shell Sabbatical, GSL Talk, GANDOLPH Proposal Funded 2006-01 Hyde, W.T., Grossman, E.L., Grossman, Crowley, T.J., Pollard, D., and Scotese, C.R., 2006. Siberian glaciation as a constraint on Permo-Carboniferous CO2 levels, Geology 34: 421-424. (100) Abstract (English): Reconstructions of Phanerozoic CO(2) levels have generally relied on geochemical modeling or proxy data. Because the uncertainty inherent in such reconstructions is large enough to be climatically significant, inverse climate modeling may help to constrain paleo-CO(2) estimates. In particular, we test the plausibility of this technique by focusing on the climate from 360 to 260 Ma, a time in which the Siberian landmass was in middle to high latitudes, yet had little or no permanent land ice. Our climate model simulations predict a lower limit for CO(2)-the value beneath which Siberia acquires 'excess' ice. Simulations provide little new information for the period in which Siberia was at a relatively low paleolatitude (360-340 Ma), but model results imply that paleo-CO(2) levels had to be greater than 2-4x modern values to be consistent with an apparently ice-free Siberia in the late Permian. These results for the later period in general agree with soil CO(2) proxies and the timing of Gondwanan deglaciation, thus providing support for a significant CO(2) increase before the end-Permian boundary event. Our technique may be applicable to other time intervals of unipolar glaciation. 2006-02 Main, D.J., and Scotese, C.R., 2006. Cretaceous North American Dinosaur Paleobiogeographic Provinces Revisited, Geological Society of America, South-Central Section, 40th annual meeting, Abstracts with Programs - Geological Society of America, v. 38, issue 1, p. 29. Abstract: The post Pangean world of the Cretaceous was a time of continued paleogeographic evolution. Tectonically, North America became connected to Eurasia via the Beringian land bridge allowing for the dispersal of dinosaurs between Asia and the Americas. Eustatically, the Late Cretaceous high stand united the interior continental seas of the Early Cretaceous and created two separate paleogeographic regions; Laramidia and Appalachia. Previous researchers have proposed dividing the North American continent into northern and southern paleobiogeographic provinces using Late Cretaceous dinosaur faunas. This project proposes to further subdivide the known paleobiogeographic provinces of Late Cretaceous dinosaurs in North America. With the development of new paleobiogeographic maps of Late Cretaceous (Campanian-Maastrichtian) dinosaur distributions, it has become apparent that North America may be further subdivided into four paleobiogeographic zones. The paleobiogeographic zones proposed are; the Northwest Laramidian, the Southwest Laramidian, the Northeast Appalachian and the Southeast Appalachian. These zones are largely established by dispersal barriers created by the Late Cretaceous high stand and the unique faunas that evolved within the separate Laramidian and Appalachian realms. A time slice series of Late Cretaceous paleobiogeographic maps will be presented that plot the distributions of dinosaurs from the Campanian to the Maastrichtian of North America. The new paleobiogeographic maps provide a framework for understanding dinosaur distributions and biogeographic provinciality during a time of continued paleogeographic change. 2006-03 Main, D.J., and Scotese, C.R., 2006. Digital Dinosaur Biogeography: Distributions and 3D Paleobiogeographic Mapping of Cretaceous Ecosystems, Sixty-sixth annual meeting of the Society of Vertebrate Paleontology, Journal of Paleontology, v. 26, issue 3, p. 94. 2006-04 Scotese, C.R., 2006. Data Behind the Plate Tectonic Modeling and How it is Managed, ESRI Petroleum User Group (PUG) Conference, April 3-5, 2006, Houston, Texas, p. 8. 2006-05 Scotese, C.R., Moore, T., Illich, H., and Zumberge, J., 2006. SourceRocker: A Heuristic Computer Program that Predicts the Occurrence of Source Rocks Using Information from Paleogeography and Paleoclimate Models, AAPG 2006 Annual Convention and Exposition, April 9-12, Houston, Texas, Abstracts: Annual Meeting - American Association of Petroleum Geologists v. 15, p. 97. Abstract: Source rocks do not occur randomly in either space or time. Rather, source rocks seem to occur more abundantly at some periods in Earth History, than at other times . Similarly, source rocks do not occur equally frequently in all depositional environments or under all climatic and oceanographic conditions. To solve the problem of source rock production in space and time, we have assembled 3D paleogeographic maps (Paleo DEMs) that model surface topography and bathymetry for eight time intervals. These topographic and bathymetric models provide the framework for paleoclimatic simulations, (FOAM) that give important information concerning the past state of the ocean and atmosphere. The results from these paleoclimatic simulations, in turn, allow us to model the key surficial processes, such as sediment transport, the depth of the mixed layer, and biological productivity, and other criteria that to a large extent control the spatial and temporal distribution of source rocks . The goal of the GANDOLPH Project is to use the artificial intelligence tools developed in SourceRocker to predict and better evaluate the potential of source rocks in basins that are under-explored or in deeply buried strata that have yet to be drilled. 2006-06 Moore, T., Scotese, C.R., Illich, H., Zumberge, J., Perlmutter, M., 2006. Climate Simulations of Hot House (Cenomanian/Turonian) and Ice House (Early Permian) Worlds: Comparisions and Contrasts, AAPG 2006 Annual Convention and Exposition, April 9-12, Houston, Texas, Abstracts: Annual Meeting - American Association of Petroleum Geologists v. 15, p.74. Abstract: During the past 600 million years the Earth's climate has alternated between Hot House conditions (no permanent polar ice cap) and Ice House conditions (polar ice cap present). In this paper we compare and contrast climate simulations for the Cenomanian/Turonian (93.5 Ma) and the Early Permian (280 Ma), respectively. The goal is to better understand: which features of the Earth's climate system are stable under these extremely different conditions, which features are most variable, how the style of equator-to-pole energy transfer changes under these two very different regimes, the relative importance of Milankovitch forcing, the correlation between source rock productivity and the global climate system, as well as the nature of the transition from Hot House to Ice House worlds, and vice versa. During the past 600 million years there have been four major Ice House worlds: Late Precambrian, Late Ordovician, PermoCarboniferous, and Late Cenozoic. In addition, there have been two minor excursions towards Ice House conditions (Late Devonian and early Cretaceous). During the Phanerozoic, the total time interval for Ice House conditions has been approximately 110 million years (20%). Either Hot House or Ice House conditions generally prevail (90% of the time). This suggests that positive feedback mechanisms drive the climate system from one climatic extreme to the other in relatively shorts period of time, geologically speaking. When the history of the Earth's climate is compared with temporal trends in source rock productivity, a positive correlation can be found between Hot House worlds and times of greater than average source rock productivity. All major Oceanic Anoxic Events (OAEs) occur during times of Hot House climate. We will consider how aspects of the Earth system (ocean, atmosphere, biosphere, cryosphere) favor source rock production during times of Hot House climate, and in particular, how Hot House climates spawn OAE events. 2006-07 Peters, K.E., Ramos, L.S., Zumberge, J.E., Scotese, C.R., and Gautier, D.L., 2006. Circum-Arctic Petroleum Systems: Data Mining and Prediction of Physical Properties Using Chemometrics and Paleoreconstruction, AAPG 2006 Annual Convention and Exposition, April 9-12, Houston, Texas, Abstracts: Annual Meeting - American Association of Petroleum Geologists v. 15, p. 84. Abstract: The Circum-Arctic is one of the last major frontiers in petroleum exploration. As part of the World Energy Consortium organized by the U.S. Geological Survey, source- and age-related biomarker and isotopic data were measured for more than 1000 crude oil and seep samples collected above 55 degrees N latitude. A unique, multi-tiered decision tree consisting of many chemometric (multivariate statistical) models created using Pirouette allowed detailed classification of genetically related oil groups. The results show that our new chemometric approach is more versatile than conventional methods for oil-oil and oil-source rock correlation. Using 622 'training set' samples, an automated protocol was created using InStep (super TM) to classify newly acquired samples of crude oils, seeps, and source-rock extracts, and assign corresponding confidence limits. The geochemical data were also used to infer the age, lithology, organic matter input, and depositional environment of the source rock for each oil sample. Twenty-one oil groups were identified, mapped, and linked to their source rocks; examples include Upper Jurassic distal marine shale (West Siberia), Lower-Middle Jurassic paralic-deltaic marine shale (West Siberia), Triassic marine marl (North Slope), Devonian fluvial lacustrine shale (Scotland), Devonian marine carbonate (Western Canada Basin), and Precambrian marine marl (East Siberia). To better assess the original and present-day distributions of each petroleum system, paleo-latitudes and paleo-longitudes of the samples were reconstructed using PointTracker and located on paleogeographic maps using Earth System History-GIS (PALEOMAP Project, C. Scotese). These paleomaps can be used to predict the physiochemical properties of discoveries within the mapped areal extent of each petroleum system, including sulfur content, API gravity, and gas-to-oil ratio. 2006-08 Nokleberg, W.J., Bundtzen, T.K., Dawson, K.M., Monger, J.W.H., and Scotese, C.R., 2006. Paleozoic and Mesozoic Metallogenic and Tectonic History of the Wrangellia Composite Terrane in Alaska and the Canadian Cordillera, Geological Society of America, Cordilleran Section, 102nd annual meeting; American Association of Petroleum Geologists, Pacific Section, 81st annual meeting; Society of Petroleum Engineers, Western Region, 76th annual meeting, 8–10 May 2006, Abstracts with Programs - Geological Society of America, v. 38, issue 5, p. 25. Abstract: The Wrangellia composite terrane (Alexander, Peninsular, and Wrangellia terranes) exhibits a long and complicated metallogenic and tectonic history. The major Paleozoic and Mesozoic metallogenic and tectonic events are: (1) Neoproterozoic formation of volcanogenic massive sulfide deposits in a back arc in the Alexander terrane; (2) Ordovician-Silurian formation of porphyry Cu-Mo and associated deposits hosted in plutons in a continental-margin arc in the Alexander terrane; (3) Middle and Late Devonian formation of kuroko massive sulfide deposits in island-arc volcanic units in the Wrangellia terrane; (4) Pennsylvanian and Permian formation of Cu skarn, porphyry Cu, and kuroko massive sulfide deposits in the Skolai island arc in the Wrangellia terrane; (5) Late Triassic formation of podiform Cr and stratiform PGE deposits in subduction-related mafic and ultramafic plutons in the basal part of the Talkeetna-Bonanza island arc in the Wrangellia terrane; and formation of gabbroic Ni-Cu, stratiform PGE, and Cyprus and Kuroko massive sulfide deposits in the Nikolai Greenstone and correlative units during back-arc rifting of the Wrangellia and Alexander terranes; (6) Earl Jurassic formation of Cu and Fe skarn, kuroko massive sulfide, and porphyry Cu and related deposits in the Talkeetna-Bonanza island arc in the Peninsular, Wrangellia, and Alexander terranes; (7) Late Jurassic formation of porphyry Cu and related deposits in the subduction-related granitoid plutons, and formation of zoned mafic-ultramafic PGE-Cr-Ti deposits in subduction-related mafic and ultramafic plutons of the Gravina island arc in Wrangellia terrane. (8) Early Cretaceous formation of porphyry Mo and associated deposits, and kuroko massive sulfide deposits in volcanic units of the Gravina island arc in Wrangellia terrane. (9) Late Early Cretaceous formation of porphyry Mo, Cu skarn, polymetallic vein, and manto deposits in the Omineca-Selwyn collisional plutonic belt that is interpreted as forming during final accretion of Wrangellia composite terrane to North American continental margin; And (10) Early Late Cretaceous formation of granitoid-related, Au- and Cu- Ag quartz vein, and Kennecott Cu deposits during anatexis and regional metamorphism associated with the final accretion of the Wrangellia composite terrane. 2006-09 Nokleberg, W.J., Scotese, C.R., and Monger, J.W.H., and 2006. Major tectonic processs illustrated in a Phanerozoic model for Alaska and the Canadian Cordillera, Geological Society of America, Cordilleran Section, 102nd annual meeting; American Association of Petroleum Geologists, Pacific Section, 81st annual meeting; Society of Petroleum Engineers, Western Region, 76th annual meeting, Abstracts with Programs - Geological Society of America, v. 38, issue 5, p. 81. Abstract: Six tectonic processes were responsible for formation of the collage of terranes and overlap assemblages in Alaska and the Canadian Cordillera. (1) In the Late Devonian and Early Mississippian, a major period of rifting occurred along the ancestral continental margin of North America. The rifting resulted in formation of an ocean basin that contained cratonal and passive continental-margin terranes that eventually migrated and accreted at other sites along the evolving margin of the continent. (2) From about the Late Triassic through the mid-Cretaceous, a succession of island arcs and tectonically paired subduction zones formed near the continental margin. (3) From about mainly the mid-Cretaceous through the present, a succession of igneous arcs and tectonically paired subduction zones formed along the continental margin. (4) From about the Jurassic to the present, oblique convergence and rotations caused orogen-parallel sinistral and then dextral displacements within the upper plate margins of the North American Craton. The oblique convergences and rotations resulted in the fragmentation, displacement, and duplication of formerly more-continuous arcs, subduction zones, and passive continental margins. These fragments were subsequently displaced along the margins of the expanding continental margin. (5) From the Early Jurassic through Tertiary, movement of the upper continental plates toward subduction zones resulted in strong plate coupling and accretion of the former, separate island arcs and subduction zones to continental margins. Accretions were accompanied and followed by crustal thickening, anatexis, metamorphism, and uplift. The accretions resulted in the substantial growth of the North American continent. (6) In the middle and late Cenozoic, oblique to orthogonal convergence of the Pacific Plate with present-day Alaska resulted in formation of the modern-day ring of volcanoes around continental margin. The oblique convergence between the Pacific Plate and Alaska also resulted in major dextral-slip faulting in interior and Southern Alaska and along the western part of the Aleutian-Wrangell arc. Associated with dextral-slip faulting was crustal extrusion of terranes from Western Alaska into the Bering Sea. 2006-10 Moore,T.L., Perlmutter, M.A., and Scotese, C.R., Impact of high frequency climate cycles on Cretaceous and Permian Climate Systems, Joint SEPM-GSL Research Conference, The Application of Earth System Modelling to Exploration, Abstracts and Program, July 11-13, 2006, Snowbird, Utah, p 52. Abstract: The distribution of source and reservoir rocks is strongly influenced by climate. Within a sedimentary basin, climate change directly influences river runoff, sediment discharge rates, organic productivity through increases and decreases in fresh water discharge, and shifts in oceanic upwelling. Although many potential short-term controls on climate exist (impacts, eruptions, and changes in the brightness of the sun), cyclic changes in Earth’s orbit can are the only ones that produce regular, repetitive climate shifts at time scales of less than 20,000 years. Earth’s orbital cycles include eccentricity (the change in orbit shape), precession (change in direction of axial tilt), and obliquity (change in axial tilt angle). Of these, precession, coupled with high eccentricity, produces the largest variation of insolation. These changes in insolation express their impact by altering seasonal temperature, evaporation, precipitation, and other aspects of climate as heat is redistributed in the ocean-atmosphere system. To fully understand the potential range of climate cycles, we conducted climate simulations for the mid Cretaceous, a green-house world with high C02, high sea level, and no land ice, and for the early Permian, a ice-house world with low C02, low sea level, and a large southern- hemisphere ice sheet. Results clearly show that periods of high summer insolation produce wetter climates (Figure 1). This relationship has a very interesting effect because the effect of precession forces the climates of the northern and southern hemispheres to be 10,000 years out of phase. When one hemisphere experiences high insolation during a summer, the opposite hemisphere has a low insolation summer, with lower rainfall. Note, that as a consequence of this shifting seasonal precipitation pattern, the arid belts also shift accordingly in opposite geographic directions. 2006-11 Scotese, C.R., Moore, T., Illich, H., and Zumberge, J., 2006. Do We Need a Wizard to Find Source Rocks?, Joint SEPM-GSL Research Conference, The Application of Earth System Modelling to Exploration, Abstracts and Program, July 11-13, 2006, Snowbird, Utah, p 61. Abstract: Source rocks do not occur randomly in either space or time. Rather, source rocks seem to occur more abundantly at some periods in Earth History, than at other times (e.g. late Silurian, late Devonian, Permo-Carboniferous, Late Jurassic, mid-late Cretaceous, Oligo-Miocene; Ulmishek and Klemme, 1990). Similarly, source rocks do not occur equally frequently in all depositional environments or under all climatic and oceanographic conditions. The most abundant deposits of source rocks (e.g., the Mideast, northern South America) appear to have been produced in tropical regions, adjacent to zones of vigorous upwelling, or at times when conditions enabling carbon preservation have been especially favored (e.g., mid-Cretaceous Oceanic Anoxic Events). We have taken an Earth System Science approach to solve the riddle of source rock production in space and time. This approach starts with high resolution 3D paleogeographic maps (Paleo DEMs) that model surface topography and bathymetry for eight time intervals. These topographic and bathymetric models provide the framework for paleoclimatic simulations, (FOAM) that give important information concerning the past state of the ocean and atmosphere. The results from these paleoclimatic simulations, in turn, allow us to model the key surficial processes, such as sediment transport, the depth of the mixed layer, and biological productivity, and other criteria that to a large extent control the spatial and temporal distribution of source rocks . To solve the problem of source rock production in space and time, we have assembled 3D paleogeographic maps (Paleo DEMs) that model surface topography and bathymetry for eight time intervals. These topographic and bathymetric models provide the framework for paleoclimatic simulations, (FOAM) that give important information concerning the past state of the ocean and atmosphere. The results from these paleoclimatic simulations, in turn, allow us to model the key surficial processes, such as sediment transport, the depth of the mixed layer, and biological productivity, and other criteria that to a large extent control the spatial and temporal distribution of source rocks . We employ spatial recognition techniques (SpotFire,Pirouette, ArcGIS - Spatial Analyst) and rule-based artificial intelligence programming to: 1) analyze the vast amount of environmental data made available by the paleoclimate simulations, 2) compare the spatial distribution of these environmental parameters with the spatial occurrence of known and inferred source rocks, 3) recognize patterns and associations within these two data sets, and 4) use these patterns and associations to build a system of rules and decision trees describing the likelihood of source rock occurrence. The goal of the GANDOLPH Project is to use these techniques to predict and better evaluate the potential of source rocks in basins that are underexplored or in deeply buried strata that have yet to be drilled. 2006-12 Zumberge, J., Illich, H., and Scotese, C., 2006. Key Oil Biomarkers Confirm Paleogeographic/Paleoclimatic Upwelling Models for the Cretaceous and Permian, Joint SEPM-GSL Research Conference, The Application of Earth System Modelling to Exploration, Abstracts and Program, July 11-13, 2006, Snowbird, Utah, p 70. Abstract: Key ratios of various tricyclic terpane biomarkers have long been know to predict source rock environmental characteristics such as 1) the influx of terrestrial organic matter [C19/C23]; 2) lithofacies - marine shale/marl/carbonate [C22/C21 and C24/C23]; and 3) lacustrine depositional settings [C26/C25] (e.g. Zumberge and Ramos, 1996 and Peters et al., 2005). Tricyclic terpanes likely represent hydrocarbon remnants of prokaryotic membrane lipids (e.g. Ourisson et al., 1982; Peters, 2000). More recently, Holba et al. (2003) reported that high proportions of extended tricyclic terpanes [C26+] nearly always occur in oils generated from source rocks deposited under upwelling regimes [e.g. Permian Phosphoria (Piper and Link, 2002), Triassic Shublik (Parrish et al., 2001), Cretaceous La Luna (Erlich et al., 2000), and Miocene Monterey (Isaacs and Rullkotter, 2001)]. Another biomarker, a C24 tetracyclic terpane, is always in relatively low abundance in marine oils when the extended tricyclic terpanes are elevated, and visa versa. High tetracyclic and low extended tricyclic terpane abundances occur in oils generated from source rocks deposited in warm, shallow water, intra-shelf basins (mostly carbonate lithofacies). Oil biomarkers known as aryl isoprenoids indicate the presence of phototrophic green sulfur bacteria (Chlorobiaceae) in the source depositional environment (Summons and Powell, 1987). A high abundance of these biomarkers suggests the source sediments were deposited under photic zone euxinic (PZE) conditions. In other words, the near surface waters were not only anoxic, but often sulphidic with significant H2S present. Aryl isoprenoids are common constituents of oils from Cretaceous marine shales deposited in the Western Interior Seaway of North America. Both the paleogeographic/paleoclimatic model and tricyclic terpane biomarkers indicate little or no major upwelling conditions for this seaway. In contrast, Cenomanian/Turonian oils derived from the La Luna and its equivalents from the SubAndean basins of northern South America have very high upwelling biomarkers, confirming the strong modeling upwelling indicators. La Luna derived Putumayo and Oriente basin oils have both elevated upwelling and PZE parameters; modeling upwelling parameters are lower than might be expected for the region. This may partly result from the paleogeography of these adjacent basins. A series of “highs” separate the Oriente and Putumayo basins from “open” ocean shelf and shelf edge areas in which upwelling is modeled to have occurred. The highs are a series of features on the western flanks of the basins over which Cretaceous section thins significantly (e.g., Macellari, 1988). “Gaps” between these features permitted influx and exchange of marine water; upwelled, nutrient-rich marine waters entering these basins from the west may account for the biomarker values in basinal settings somewhat remote from areas of significant modeled upwelling. The occurrence of high PZE values may additionally be rationalized in terms of Cretaceous paleogeography. Periodic eustatic or tectonic interruption of water exchange between Oriente and Putumayo basins and normal marine environments may have promoted episodes of stagnation, and the evolution of euxinic conditions. Permian Phosphoria oils from various Wyoming basins also have strong upwelling biomarker signatures with no PZE biomarkers. The Phosphoria was deposited on the western margin of Pangea, some 15° north of the paleo-equator, a region with strong modeled upwelling conditions. Earlier Permian oils (Leonardian) from West Texas and New Mexico were generated from marine carbonates and marls (Hill et al., 2004), also deposited near the western margin of Pangea, on or near the paleo-equator. Some of these petroleum systems have PZE signals but week upwelling biomarkers. Again, this can be related to paleogeographic restrictions. 2006-13 Metzler, S., and Scotese, C.R., 2006. Ophiolite formation and obduction during the Phanerozoic and Late Precambrian, Geological Society of America 2006 Annual Meeting, October 22-25, Philadelphia, PA, Abstracts with Program, v. 38, issue 7, p. 212. Abstract: Ophiolites, tectono-stratigraphic assemblages of ancient oceanic crust are one of the key lines of evidence used to reconstruct ancient ocean basins and to constrain the timing of the collisional events that closed these ocean basins. We have assembled an ArcGIS (ESRI) database that describes the geographic and chronologic occurrences of more than 300 ophiolite localities, worldwide. The attributes of each ophiolite locality include: 1) the age of the formation of the ocean floor comprising the ophiolite, 2) the tectonic setting in which the ocean floor was formed (i.e., mid-ocean ridge vs. back-arc basin), 3) the age of obduction of the ophiolite, and 4) the tectonic setting of ophiolite obduction (e.g., continent-continent collision, back-arc basin collapse). A completeness score was also given for each ophiolite indicating how many of the seven classic ophiolite components were observed. Using ArcMap, the ophiolite localities were plotted on a set of 40 plate tectonic reconstructions assembled by the PALEOMAP Project. These maps illustrate the changing location of ancient spreading centers, subduction zones, island arcs, seamounts, and oceanic plateaus since the late Precambrian. An attempt was made to show both the timing and location of ophiolite obduction, and a speculative estimate of where the oceanic crust comprising the ophiolite originally formed. This was done by "back-tracking" plate motions. An animated version of these maps will be presented. In general, the data that we have compiled indicate that ophiolites did not form uniformly in space and time. Rather, there are times when ophiolite formation and emplacement were more likely. As other authors have proposed, 1) the oceanic crust that makes up most ophiolites often forms near subduction zones, probably in back arc basins and island arcs, 2) the age of oceanic crust formation usually precedes the time of ophiolite obduction by less than 20 million years of each other, and 3) it seems likely that most ophiolites form as a result of back-arc basin collapse, which may be a precursor of continent-continent collision. 2006-14 Main, D., and Scotese, C.R., 2006. Dinosaur biogeography during the Mesozoic, Geological Society of America 2006 Annual Meeting, October 22-25, Philadelphia, PA, Abstracts with Program, v. 38, issue 7, p. 444. Abstract: More than 1000 genera of dinosaurs have been described from over 5000 localities worldwide (Weishampel et al., 2005). We have built an ArcGIS (ESRI) database that uses the spatial, temporal and cladistic information contained in the Weishampel compilation to plot the changing distribution of dinosaur clades on a new set of 16 paleogeographic maps for the Mesozoic: Triassic (2 maps), Jurassic (6 maps) and Cretaceous (8 maps). The goal of this project is to analyze the tempo and mode of dinosaur evolution from a biogeographic point-of-view. The new paleogeographic maps illustrate the changing configuration of the continents and ocean basins, map out ancient climatic belts, and describe how ephemeral corridors and barriers to migration opened and closed as a consequence of sea level fluctuations and topographic changes. The maps, which are based on paleo-digital elevation models (paleo-DEMs,) are especially useful for visualizing the trans-polar migration routes that played an important role in dinosaur dispersal. In this talk we will describe how the maps and ArcGIS dinosaur database was assembled, and review the broad biogeographic patterns of dinosaur vicariance and dispersal during the Mesozoic. 2006-15 Jacobs, B., Pan, A., and Scotese, C.R., 2006. Cenozoic Vegetation Change in Africa: A Large-scale View of a Small-scale Process, Geological Society of America 2006 Annual Meeting, October 22-25, Philadelphia, PA, Abstracts with Program, v. 38, issue 7, p. 381. Abstract: Relying on plant fossils to represent the evolution of Cenozoic African biomes renders a view of past vegetation biased toward geographic areas and time intervals that preserve the most specimens or had the most research. Africa is roughly three times the size of the U. S. yet is documented by only a handful of Paleogene plant localities, and has a Neogene record biased toward the depositional basins of the East African Rift. Placing all known paleobotanical sites in their correct location on paleogeographic maps helps illustrate the varied data coverage. Efforts to improve this record, which is also uneven with respect to time control, have produced Eocene, Oligocene, and Miocene sites in Tanzania, Ethiopia, and Kenya. These enrich our understanding of the history of modern plant communities, illustrate how they may have differed in the past, and provide dated paleoclimate for these intervals. A middle Eocene (46 Ma) site demonstrates that northern Tanzania (12 degrees S paleolatitude) had a dry climate similar to today, and woodland communities dominated by microphyllous, caesalpinioid legumes--structurally similar to modern woodland communities. Paleobotanical sites on the northwestern Ethiopian Plateau (11 degrees N paleolatitude) dated at 28-27 Ma document forest communities with genera found today in West Africa, and the coastal and Eastern Arc Mountains of Kenya and Tanzania, but now absent from Ethiopia. The fossils document a biogeographic link between these now disjunct genera. But, the common occurrence of palm fossils indicates these forests differed from living counterparts, where palms are always absent or species-poor. Thus, a decline in the ecological role for palms took place after 27 Ma. A decrease in palm diversity seems to have occurred before 28 Ma as the palm genera identified are found in Africa today. The Miocene record from the Tugen Hills, Kenya, indicates considerable variation in environments between 12.6 and 7 Ma, ranging from lowland forest with West African botanical affinities (including absence of palms), to seasonally dry, legume-dominated woodland or wooded savanna. These sites demonstrate the overall trend toward increasing aridity and spreading grass-dominated environments during the Neogene was complicated by smaller-scale variations in landscape and vegetation in the East African rift. 2006-16 Scotese. C.R., Reese, T., Thompson, R., Sutton, C., Bammel, B., and Ward, D., 2006. Geologists of the World, Unite!, Geological Society of America 2006 Annual Meeting, October 22-25, Philadelphia, PA, Abstracts with Program, v. 38, issue 7, p.142. (100a) was this published separately elsewhere? Abstract: A global geology website has been built that is both an archive of stratigraphic information and a portal to the geology of the world. Like a cross between Google Maps and Wikipedia, globalgeology.com, uses a geological map of the world (1:10,000,000) as an interface to help users locate and enter geological information. This information includes not only stratigraphic descriptions, but also digital images of outcrops and stratigraphic sections, and links to supporting earth science websites. The information stored at global geology.com comes in small part from legacy databases such as the Paleogeographic Atlas Project Lithologic database, the Paleobiology database, and the PALEOMAP Project Lithologic Indicators of Climate database (over 250,000 combined entries). The bulk of the information, however, comes from the worldwide community of geologists, and like Wikipedia, the global geology website is an editable, community effort. The concept is simple and is based on the premise that every geologist has a favorite outcrop or intimately knows the geology of a few special places. After selecting the appropriate time interval from an international stratigraphic time chart, a geologist can enter information about this patch of geology using an interface made up of check-boxes, drop down menus and text-boxes. This information is stored in an SQL database and the geological map of the world and the stratigraphic time chart are updated indicating that new data has been archived. If another visitor to the global geology website selects the same time-patch, he can review the geological information on-line, download the information, or enter an updated record. As the number registered users increases and as more geological information is entered, the individual patches of geological information will merge to form a nearly complete four-dimensional map and database describing the geology of the world through time. The global geology website can be accessed at www.globalgeology.com, or through the PALEOMAP Project portal at www.scotese.com. 2006-17 Scotese, C.R., and Zumberge, J., 2006. Neoproterozoic Plate Tectonic, Paleogeographic and Paleoclimatic Reconstructions: The Habitat of the Oldest Oil Accumulations, Infracambrian Hydrocarbon System Meeting and the Emerging Potential in North Africa, Geological Society of London, London, November 29-30, 2006. 2006-18 Hyde, W.T., Grossman, E.L., Crowley, T.J., Scotese, C.R., and Peltier, W.R., 2006. Past glaciations as a constraint on Phanerozoic CO2 levels, American Geophysical Union 2006 Fall Meeting, Eos, Transactions, American Geophysical Union, v. 87, Abstract PP23E-02. 2006-19 CRS Huston PUG no abs 2006-20 Haq Poster find &scan 2007 2007-01 Scotese, C.R., 2007. Paleogeographic maps of 200 Ma, 100 Ma, 0 Ma, +50 Ma future, and +250Ma future (Pangea Ultima) in William J. Broad, Long-term Global Forecast? Fewer Continents, Science Times, p. D1 and D4, New York Times, Tuesday, January 9, 2007, New York, NY. no abs 2007-02 Nokleberg, W.J., Parfenov, L.M., Monger, J.W. H., Stone, D.B., Scotese, C.R., and Scholl, D.W., 2007. Correlative geologic and tectonic events in the Russian Northeast, Alaska, and the northern Canadian Cordillera, Geological Society of America, Cordilleran Section, 103rd annual meeting, Abstracts with Programs - Geological Society of America, v. 39, issue 4, p. 60. Abstract: Six processes overlapping in time were responsible for most of the complexities of the collage of terranes and overlap assemblages around the Circum-North Pacific. (1) In the Late Proterozoic, Late Devonian, and Early Carboniferous, major periods of rifting occurred along the ancestral margins of present-day Northeast Asia and northwestern North American. The rifting resulted in fragmentation of each continent, and formation of cratonal and passive continental-margin terranes that eventually migrated and accreted to other sites along the evolving margins of the original or adjacent continents. (2) From about the Late Triassic through the mid Cretaceous, a succession of island arcs and tectonically paired subduction zones formed near continental margins. (3) From about mainly the mid-Cretaceous through the present, a succession of igneous arcs and tectonically paired subduction zones formed along the continental margins. (4) From about the Jurassic to the present, oblique convergence and rotations caused orogen-parallel sinistral and then dextral displacements within the upper plate margins of cratons that have become Northeast Asia and the North America. The oblique convergences and rotations resulted in the fragmentation, displacement, and duplication of formerly more continuous arcs, subduction zones, and passive continental margins. These fragments were subsequently accreted along the margins of the expanding continental margins. (5) From the Early Jurassic through Tertiary, movement of the upper continental plates toward subduction zones resulted in strong plate coupling and accretion of the former island arcs and subduction zones to continental margins. Accretions were accompanied and followed by crustal thickening, anatexis, metamorphism, and uplift. The accretions resulted in the substantial growth of the North Asian and North American continents. (6) In the middle and late Cenozoic, oblique to orthogonal convergence of the Pacific Plate with present-day Alaska and Northeast Asia resulted in formation of the modern-day ring of volcanoes around the Circum-North Pacific. Oblique convergence between the Pacific Plate and Alaska also resulted in major dextral-slip faulting in interior and Southern Alaska and along the western part of the Aleutian-Wrangell arc. 2007-03 Peters, K.E., Ramos, L.S., Zumberge, J.E., Valin, Z.C., Scotese, C.R., and Gautier, D.L., 2007. Circum-Arctic petroleum systems identified using decision-tree chemometrics, AAPG Bulletin, June 2007. v. 91, no. 6, 877-913. 9 (102) Abstract: Source- and age-related biomarker and isotopic data were measured for more than 1000 crude oil samples from wells and seeps collected above approximately 55 degrees N latitude. A unique, multitiered chemometric (multivariate statistical) decision tree was created that allowed automated classification of 31 genetically distinct circum-Arctic oil families based on a training set of 622 oil samples. The method, which we call decision-tree chemometrics, uses principal components analysis and multiple tiers of K-nearest neighbor and SIMCA (soft independent modeling of class analogy) models to classify and assign confidence limits for newly acquired oil samples and source rock extracts. Geochemical data for each oil sample were also used to infer the age, lithology, organic matter input, depositional environment, and identity of its source rock. These results demonstrate the value of large petroleum databases where all samples were analyzed using the same procedures and instrumentation. 2007-04 Chatterjee, S. and C. Scotese. 2007.   Biogeography of the Mesozoic Lepidosaurs on the wandering Indian plate, in Paleontologia: Cenários de Vida, I.S. Carvalho, R.C.T. Cassab, C. Schwanke, M.A. Carvalho, A.C. Fernandes, M.A.C. Rodrigues, M.S.S. Carvalho, M. Arai, and M.E.Q. Oliveira, (editors), pp. 559-587. Editoria Interciência, Rio de Janeiro, Brazil. (103) The Mesozoic lepidosaurian history in Gondwana is poorly understood because of the incompleteness of the vertebrate fossil record. Recent discoveries of three distinct lepidosaur- bearing horizons from India offer insight into the early radiation and paleobiogeography of this group in a plate tectonic framework. A plate tectonic analysis of lepidosaurian history in Gondwana reveals a sequence of events that began in the Middle Jurassic and continues to the present day. The key events in the formation of the Indian plate were: separation from Africa in the Middle Jurassic (180 Ma), separation from Madagascar and the start of its northward motion towards Asia in the Cenomanian (90 Ma), collision with ‘Greater Somalia’ at the end of the Cretaceous (-70 Ma), separation from the Seychelles and Mascarene bank at the Cretaceous- Tertiary boundary (65 Ma), and the initial collision with Asia in the Eocene (50 Ma). In this paper we focus on the plate tectonic history of India and how the successive fragmentation of the Indian plate provides an interesting biogeographic framework for testing the models of vicariance and geodispersal. A major question of Indian paleobiogeography is how the terrestrial vertebrates such as lepidosaurs responded to the tectonic evolution of the Indian plate. The earliest iguanian lizards Tikiguania from India have been recently discovered from the Late Triassic Tiki Formation (-237 Ma), when India was till part of Pangea. Tikiguania predates known records of iguanian lizards by some 60 My. The Middle Jurassic Kota Formation (-170 Ma) has yielded sphenodontians such as Rebbanasaurus and Godavarisaurus, an iguanian agamid lizard Bharatagama, and an indeterminate pleurodont lizard Paikasisaurus. Both plate tectonic and paleontologic data indicate that throughout the Late Cretaceous India was not an isolated continent, but maintained physical connections with adjacent lands. The Maastrichtian Intertrappean Beds (-66 Ma) intercalated with the Deccan Trap lava flows have produced three snakes: a cholophidian, a nigerophiid Indophis, and an inderminate taxon. An anguid lizard is also reported from these beds. Many groups of anguimorphs such as snakes and anguid lizards have disjunct distribution during the Maastrichtian, but the geodispersal corridor—Greater Somalia between Africa and India—appears to have allowed faunal exchanges between these landmasses. These squamate fossils indicate that India was not an isolated continent during the Late Cretaceous Period, but maintained biotic connection with Africa and Laurasia. Around 65 Ma at the Cretaceous/Tertiary (KT) boundary, western India was ground zero for the Deccan volcanism and the Shiva impact that may be linked to the dinosaur extinction. Because of the Shiva impact, the Seychelles microcontinent began to separate from India at the KT boundary. During the Paleocene, India acting like a giant ‘Viking Funeral Ship’ filled with its impoverished Gondwana fauna after the KT extinction, accelerated its northward journey, and docked with Asia. The collision between India and Asia in the Eocene opened a new northeastern geodispersal corridor, and several squamates were introduced into Asia. 2007-05 Rees, A., Alroy, J., Scotese, C.R., Memon, A., Rowley, D.B., Parrish, J.T., Weishampel, D.B., Platon, E., O’Leary, M.A., and Chandler, M.A., 2007. Phanerozoic Earth and life; the Paleointegration Project, Geoinformatics 2007; Data to Knowledge, USGS Scientific Investigations Report, SIR 2007-5199, p. 88-89. 2007-06 Sewall, J.O., van de Wal, R.S.W., van der Zwan, K., van Oosterhout, Dijkstra, H.A., and Scotese, C.R., 2007, Climate model boundary conditions for four Cretaceous time slices, Climate of the Past, 3:647-647, www.climat-past.net/3/647/2007/ (101) Abstract: General circulation models (GCMs) are useful tools for investigating the characteristics and dynamics of past climates. Understanding of past climates contributes significantly to our overall understanding of Earth's climate system. One of the most time consuming, and often daunting, tasks facing the paleoclimate modeler, particularly those without a geological background, is the production of surface boundary conditions for past time periods. These boundary conditions consist of, at a minimum, continental configurations derived from plate tectonic modeling, topography, bathymetry, and a vegetation distribution. Typically, each researcher develops a unique set of boundary conditions for use in their simulations. Thus, unlike simulations of modern climate, basic assumptions in paleo surface boundary conditions can vary from researcher to researcher. This makes comparisons between results from multiple researchers difficult and, thus, hinders the integration of studies across the broader community. Unless special changes to surface conditions are warranted, researcher dependent boundary conditions are not the most efficient way to proceed in paleoclimate investigations. Here we present surface boundary conditions (land-sea distribution, paleotopography, paleobathymetry, and paleovegetation distribution) for four Cretaceous time slices (120 Ma, 110 Ma, 90 Ma, and 70 Ma). These boundary conditions are modified from base datasets to be appropriate for incorporation into numerical studies of Earth's climate and are available in NetCDF format upon request from the lead author. The land-sea distribution, bathymetry, and topography are based on the 1 degrees X1 degrees (latitudeXlongitude) paleo Digital Elevation Models (paleoDEMs) of Christopher Scotese. Those paleoDEMs were adjusted using the paleogeographical reconstructions of Ronald Blakey (Northern Arizona University) and published literature and were then modified for use in GCMs. The paleovegetation distribution is based on published data and reconstructions and consultation with members of the paleobotanical community and is represented as generalized biomes that should be easily translatable to many vegetation-modeling schemes. 2007-07 Scotese, C.R., Main, D., Goswami, A., Rees, P.A., Noto, C.R., Weishampel, D.B., 2007. A Cladistic Approach to Dinosaur Biogeography: New Maps, New Patterns, and New Ideas. Soc. Vertebrate Paleontology Annual Meeting, Austin, Texas. 2007-08 Scotese, C.R., Illich, H., Zumberge, J, and Brown, S., 2007. The GANDOLPH Project: Year One Report: Paleogeographic and Paleoclimatic Controls on Hydrocarbon Source Rock Deposition, A Report on the Methods Employed, the Results of the Paleoclimate Simulations (FOAM), and Oils/Source Rock Compilation, Conclusions at the End of Year One, February, 2007. GeoMark Research Ltd, Houston, Texas, 142 pp. fix formatting errors 2007-09 Scotese, C. R., 2007. Paleogeographic maps of 250 Ma, 150 Ma, 0 Ma, +150 Ma future, and +150 Ma future (Pangaea Proxima) on p 137-138, in Une projection a 250 millions d’annees: Un seul continent, un Seul?, by William J. Broad, GEO Magazine, April, 2007, number 338, p. 136-139. no abs 2007-10 Moore, T.L., Perlmutter, M., and Scotese, C.R., 2007. Using climate model experiments of orbital cycles to understand stratigraphic variability, AAPG 2007 annual convention & exhibition, Abstracts: Annual Meeting - American Association of Petroleum Geologists, v. 2007, p. 97. Abstract: Climate in general plays a role in the distribution of stratigraphic intervals, including reservoir and source rocks, by impacting sediment yield and productivity. However, climate is not static over the time interval these rocks form. Both long-term controls (such as continental geography) and short-term controls (such as orbital cycles or unique events) can all impact climate and deposition. Of these, the short-term controls are often the most difficult to assess because their effects are often below the time resolution of the strata. We used the FOAM model to run multiple sets of orbital parameters to evaluate short-term change. The parameters chosen covered a range of obliquity, eccentricity, and precession states. From the results of modeling, we assessed (1) the impacts of orbital cycles on precipitation in river systems and upwelling and (2) the potential rate of variation through time. We concentrated on the Cretaceous (Cenomanian/Touronian) and the Early Permian to evaluate two climatic extremes (hot and ice houses, respectively). The results of modeling showed that (1) the interaction between eccentricity and precession generated the largest climate variation; (2) when eccentricity is high, relatively small changes in precession, 25% of a cycle (less than 5 kyr), can produce the largest differences; (3) the major atmospheric circulation cells can shift several degrees of latitude, impacting precipitation and wind patterns; and (4) environments such as deserts and rainforests vary in size and geographic range as circulation cells shift. This work clearly demonstrates (1) the rate at which large paleoclimatic changes occurs is much faster than is commonly recognized and (2) the full range of high-frequency climate changes impacting an area need to be investigated when interpreting stratigraphy. 2007-11 Scotese, C. R., 2007. +50 Ma future, 150 Ma future, and +250 Ma Future maps on pp. 17, 20 - 21, in Kohti uuta Pangaia by Eeva Makela, Tiede: elamysia uteliaalle, September, 2007, p. 16-21. no abs 2007-12 Peters, K., Ramos, S., Zumberge, J., Valin, Z., and Scotese, C., 2007. Chemometric restoration of source-rock paleogeography using biomarker and isotope compositions of crude oils, 23rd International Meeting on Organic Chemistry, September 9-14, Torquay, England, Final Programme, Abstract of Reports, v. 23, p. 911-912. 2007-13 Zumberge, J., Illich, H., and Scotese, C.R., 2007. Biomarkers from Marine Crude Oils Reflect Modeled Climatic/Oceanographic Conditions for the Late Cretaceous, 23rd International Meeting on Organic Chemistry, September 9-14, Torquay, England, Final Programme, Abstract of Reports, v. 23, p. 555. 2007-14 Scotese, C. R., 2007. Pangaea Proxima map on p. 39, in Pangaea, the comeback (cover story), New Scientist, October 20, 2007, p. 37 - 40. no abs 2007-15 Goswami, A., Scotese, C.R., and Moore, T., 2007. Time continuous Climate Models for the Cretaceous, American Geophysical Union 2007 Fall Meeting, December 10-14, San Francisco, Eos, Transactions, American Geophysical Union, v. 88, issue 52, Abstract PP23B-1343. Abstract: Conventional paleoclimate studies use a “timeslice” approach in which climate simulations are run for a particular time interval (e.g. KT, 66 Ma), often evaluating the sensitivity of the model to changes in atmospheric chemistry or orbital state. Each of these simulations often takes weeks of computer time. In addition, each simulation only represents climate for about 100 years during a “timeslice” interval that could represent millions of years. These standard approaches, while very useful, have limited applicability for understanding the tectonic impacts on climate. We present a new approach called “Time Continuous” Climate Modeling (TCCM). This approach is designed to evaluate global and regional climatic changes as continents slowly move, mountains ranges are built and eroded, and mid-ocean ridges and subduction zones move. To evaluate the impacts of these slow changes, simulations are run over closely spaced time intervals (1-5 million years). At such high-resolution time steps, we will be able to detect climatic tipping points, the importance of subtle changes in geography, and the climatic evolution of continents as they move across the globe. The TCCM approach is made possible by the use of: 1) high-performance linux clusters 2) more efficient climates models (i.e., FOAM) and, 3) the availability of paleogeographic and paleobathymetric maps at one million year intervals (PALEOMAP Project). The initial time slice simulation, in this case the Late Cretaceous (66 Ma), is a standard 100-year coupled run. Each subsequent simulation, however, substitutes the geography and uses the end climatic results as an initial climatic condition of the previous simulation. This new simulation, since the geography and other parameters were highly similar to the previous run, should stabilize sooner than the initial run and thus require few model years, possibly as few as 10 years. Should instabilities develop, a full simulation, or ocean-only simulations can be run through the sequence of time slices. This method provides basic understanding of climatic evolution over longer time scales while limiting cost in time and money. 2007-16 Brown, S., Scotese, C.R., Illich, H., and Zumberge, J., 2007. GANDOLPH: Paleogeographic and Paleoclimatic Controls on Hydrocarbon and Source Rock Deposition, Year 3 & 4 Proposal, GeoMark Research Ltd, Houston, Texas, 8 pp. 2007-17 Scotese, C.R., Illich, H., Zumberge, J, and Brown, S., and Moore, T., 2007. The GANDOLPH Project: Year One Report: Paleogeographic and Paleoclimatic Controls on Hydrocarbon Source Rock Deposition, A Report on the Methods Employed, the Results of the Paleoclimate Simulations (FOAM), and Oils/Source Rock Compilation, Conclusions at the End of Year One: Cenomanian/Turonian (93.5 Ma), Kimmeridgian/Tithonian (151 Ma), Sakmarian/Artinskian (284 Ma), Frasnian/Famennian (375 Ma), February, 2007. GeoMark Research Ltd, Houston, Texas, 142 pp. 2007-18 Scotese, C.R., and Danforth, A., 2007. Plate Tectonic Evolution of the Circum-African Margins, in “Africa: Path to Discovery”, 4th HGS/PESGB International Conference on African Exploration and Production, September 7-8, Houston, Texas. Abstract: Four computer animations are presented that illustrate the principal plate tectonic events that shaped the African continent: 1) the Pan-African assembly of the Precambrian terranes, 2) the early to late Jurassic rifting in the Somali and Mozambique basins that formed the eastern and southeastern margins of Africa, 3) the late Jurassic through late Cretaceous evolution of the Central and South Atlantic margins and, 4) the late Cenozoic evolution of the Red Sea, Gulf of Aden, and the East African Rift System. The animations are based on a comprehensive and detailed computer model describing the plate tectonic evolution of the Circum-African margins. This plate tectonic model has two components. The first component is a non-traditional tectonic map of Africa that describes the tectonic features of Africa in terms of “plate polygons”. Each polygon represents a chunk of African lithosphere that has had an independent history of motion (e.g., a thrust sheet, accreted terrane, stretched continental margin). Over 1,000 plate polygons have been mapped. The second component of the plate tectonic model is a “tectonic hierarchy” that describes the relative motion between the plate polygons through time. Similar to a “plate circuit”, this hierarchical tectonic model uses total finite rotations to describe the relative motions between pairs of plate polygons. ArcGIS software has been used to produce the animations and is also being used to produce a new “Circum-African Plate Tectonic Atlas”. GIS software included with the Atlas allows users to overlay and reconstruct any modern geological, geophysical or geographical data set on top of the plate tectonic base maps. The animations presented here represent our current state of knowledge of the plate tectonic history of Africa. We have embarked on a collaborative research effort to refine and update the plate tectonic model, with a goal of describing the tectonic evolution of the African margins from the late Permian to the present-day. Critical review of the work in progress is welcomed and collaboration is invited. 2008 2008-01 Nokleberg, W. J., Parfenov, L. M., Scotese, C. R., Badarch, G. Berzin, N. A., Khanchuk, A. I ., Kuzmin, M. I., Obolenskiy, A. A., Prokopiev, A. V., Rodionov, S. M., Yan Hongquan, Tectonic and metallogenic evolution of Northeast Asia, 2008. 33rd International Geological Congress, Norway, 2008, International Geological Congress, Abstracts, v. 33, Abstract 1342127. Abstract: The vast, mountainous terranes of Northeast Asia hold the key to the tectonic and metallogenic evolution of a major and geologically complicated region of the world. This region stretches from the Ural Mountains and the Arctic Islands of central Russia to the Kamchatka volcanic arc in the Russian Far East. The region also includes northern Kazakhstan, China, Mongolia, the Korean Peninsula, and Japan. The tectonic development of the region is recorded in a series of cratons, craton margins, oceanic plates, active rifts, and orogenic collages of the present-day Northeast Asia continent. The collages consist of tectonostratigraphic terranes that are com-posed of fragments of igneous arcs, accretionary-wedge and subduction-zone complexes, passive continental margins, and cratons. The tectonostratigraphic terranes are overlapped by continental-margin-arc and sedimentary-basin assemblages. The tectonic history of cratons, craton mar-gins, oceanic plates, terranes, and overlap assemblages is complex due to extensional dispersion and translation during strike-slip faulting that occurred subparallel to continental margins. This talk presents a series of regional tectonic time-slice maps and a computer animation that dynamically illustrate the tectonic assembly and major metallogenic events of Northeast Asia since the late Precambrian. The key events in the tectonic history of Northeast Asia are: (1) the formation of the North Asian Craton during the breakup of a late Precambrian supercontinent; (2) during the late Precambrian and early Paleozoic, establishment of an active subduction zone along the present-day, southern margin of the North Asian Craton (Mongolian subduction zone); (3) during the late Paleozoic, closure of oceans between Siberia, Baltica, Kazakhstan, and north China; (4) during the Triassic and Jurassic, progressive closure of the Mongol-Okhotsk Ocean between Sino-Korean and the North Asian Cratons to form the core of present-day North-east Asia; (5) during the Late Jurassic through early Cenozoic, accretion of allochthonous terranes along the northern margin of the North Asian Craton, and along the margin of Eastern Asia; (6) for the first time in the early Cretaceous, formation of a continuous continental complex between the Russian Northeast and northwestern North America; and finally (7) in the Cenozoic, formation of continental-margin arcs and back-arc basins along the entire Pacific-facing margin of Northeast Asia. These time-slice maps provide the basis of a preliminary dynamic tectonic and metallogenic model of Northeast Asia that as an animation provides new insights into the geologic, tectonic, and metallogenic evolution of this complex region. 2008-02 Peters, K. E;., Ramos, L. S., Zumberge, J. E., V. Zenon, C., Scotese, C. R., 2008. Restoration of Circum-Arctic Upper Jurassic source rock paleolatitude based on crude oil geochemistry, 23rd International Meeting on Organic Geochemistry, United Kingdom, Organic Geochemistry, v. 39, issue 8, p. 1189-1196. wrong Abstract: The Phanerozoic metallogenic and tectonic evolution of the Circum-North Pacific (Russian Far East, Alaska, and the Canadian Cordillera) is recorded in the cratons, craton margins, and orogenic collages of the Circum-North Pacific mountain belts that separate the North Pacific from the eastern North Asian and western North American Cratons. The collages consist of tectonostratigraphic terranes with older metallogenic belts that are composed of fragments of igneous arcs, accretionary-wedge and subduction-zone complexes, passive continental margins, and cratons; they are overlapped by continental-margin-arc and sedimentary-basin assemblages with younger metallogenic belts. The metallogenic and geologic history of terranes, overlap assemblages, cratons, and craton margins is highly complicated because of post-accretion dismemberment and translation during strike-slip faulting that occurred subparallel to continental margins. Six processes overlapping in time were responsible for most metallogenic and geologic complexities of the region. (1) In the Late Proterozoic, Late Devonian, and Early Carboniferous, major periods of rifting occurred along the ancestral margins of present-day Northeast Asia and northwestern North American. (2) From about the Late Triassic through the mid-Cretaceous, a succession of island arcs and contained igneous-arc-related metallogenic belts, and tectonically paired subduction zones formed near continental margins. (3) From about mainly the mid- Cretaceous through the present, a succession of igneous arcs and contained metallogenic belts, and tectonically paired subduction zones formed along the continental margins. (4) From about the Jurassic to the present, oblique convergence and rotations caused orogen-parallel sinistral, and then dextral displacements within the upper plate margins of cratons that have become Northeast Asia and the North America. (5) From the Early Jurassic through Tertiary, movement of the upper continental plates toward subduction zones resulted in strong plate coupling and accretion of the former island arcs, subduction zones, and contained metallogenic belts to continental margins. (6) In the middle and late Cenozoic, oblique to orthogonal convergence of the Pacific Plate with present-day Alaska and Northeast Asia resulted in formation of the modern-day ring of volcanoes and contained metallogenic belts around the Circum-North Pacific. To illustrate the Phanerozoic metallogenic and tectonic evolution of the Circum-North Pacific, dynamic computer animation with successive time-stage diagrams for the region is constructed to portray the formation of metallogenic belts and associated tectonic events through geologic space and time. 2008-03 Nokleberg, W. J., Bundtzen, T. K., Scotese, C. R., Parfenov, L. M., Monger, J. W. H., Dawson, K. M., Khanchuk, A. I., Goryachev, N. A., Shpikerman, V. I., 2008. Metallogenic and tectonic model for the Circum-North Pacific, 33rd International Geological Congress, Norway, 2008, International Geological Congress, Abstracts, v. 33, Abstract 1342108. Abstract: The Phanerozoic metallogenic and tectonic evolution of the Circum-North Pacific (Russian Far East, Alaska, and the Canadian Cordillera) is recorded in the cratons, craton margins, and orogenic collages of the Circum-North Pacific mountain belts that separate the North Pacific from the eastern North Asian and western North American Cratons. The collages consist of tectonostratigraphic terranes with older metallogenic belts that are composed of fragments of igneous arcs, accretionary-wedge and subduction-zone complexes, passive continental margins, and cratons; they are overlapped by continental-margin-arc and sedimentary-basin assemblages with younger metallogenic belts. The metallogenic and geologic history of terranes, overlap assemblages, cratons, and craton margins is highly complicated because of post-accretion dismemberment and translation during strike-slip faulting that occurred subparallel to continental margins. Six processes overlapping in time were responsible for most metallogenic and geologic complexities of the region. (1) In the Late Proterozoic, Late Devonian, and Early Carboniferous, major periods of rifting occurred along the ancestral margins of present-day Northeast Asia and northwestern North American. (2) From about the Late Triassic through the mid-Cretaceous, a succession of island arcs and contained igneous-arc-related metallogenic belts, and tectonically paired subduction zones formed near continental margins. (3) From about mainly the mid- Cretaceous through the present, a succession of igneous arcs and contained metallogenic belts, and tectonically paired subduction zones formed along the continental margins. (4) From about the Jurassic to the present, oblique convergence and rotations caused orogen-parallel sinistral, and then dextral displacements within the upper plate margins of cratons that have become Northeast Asia and the North America. (5) From the Early Jurassic through Tertiary, movement of the upper continental plates toward subduction zones resulted in strong plate coupling and accretion of the former island arcs, subduction zones, and contained metallogenic belts to continental margins. (6) In the middle and late Cenozoic, oblique to orthogonal convergence of the Pacific Plate with present-day Alaska and Northeast Asia resulted in formation of the modern-day ring of volcanoes and contained metallogenic belts around the Circum-North Pacific. To illustrate the Phanerozoic metallogenic and tectonic evolution of the Circum-North Pacific, dynamic computer animation with successive time-stage diagrams for the region is constructed to portray the formation of metallogenic belts and associated tectonic events through geologic space and time. 2008-04 Tabor, N.J., Montañez, I.P., and Scotese, C.R., Mack, G.H., and Poulsen, C.J.,2008. Paleosol Archives of Environmental and Climatic History in paleotropical Western Pangea during the latest Pennsylvanian through Early Permian, in Resolving the Late Paleozoic Ice Age in time and space, Fielding, C.R., Frank, T.D., and Isbell, J.L. (editors.). Special Paper - Geological Society of America, v.. 441, pp. 291-303. (107) Abstract: The stratigraphic and regional distributions of paleosol morphology in latest Pennsylvanian through Early Permian strata in Colorado, Utah, Arizona, New Mexico, Texas, and Oklahoma are presented in this paper. This regional extent corresponds to a paleolatitudinal gradient spanning approximately 5 degrees S to 10 degrees N. Morphological trends from this region delineate significant and systematic temporal and spatial changes in Permian-Carboniferous paleoenvironment and paleoclimate. The inferred latest Pennsylvanian (Virgilian) through early Early Permian environmental pattern is complex, but it indicates persistently dry, semiarid to arid conditions in Colorado, Utah, and Arizona, at paleolatitudes north of approximately 2 degrees N, whereas lower paleolatitude (approximately 2 degrees S to 2 degrees N) tropical regions in New Mexico exhibit a stepwise shift from subhumid to semiarid and variably seasonal conditions throughout late Pennsylvanian and the first half of Early Permian (Virgilian through Wolfcampian) time, followed by a subsequent shift to more arid conditions during the latter part of the Early Permian (Leonardian). Notably, strata from the southernmost paleosites, in Texas and Oklahoma, exhibit the most significant and abrupt climate changes through this period; they show a rapid transition from nearly ever-wet latest Pennsylvanian climate (at approximately 5 degrees S) to drier and seasonal climate across the Permian-Carboniferous system boundary, and finally to arid and seasonal climate by Leonardian time (at approximately 2-4 degrees N). The inferred climate patterns show no robust long-term correlation with the high-latitude Gondwanan records of glaciation. Rather, the long-term record of Permian-Pennsylvanian climate indicators from the southwestern United States is most simply explained by an approximately 8 degrees northward tectonic drift through (essentially) static climate zones over western tropical Pangea during the interval of study. However, the relatively rapid perturbations to climate recorded by these pedogenic archives appear to be too rapid for tectonic forces and might correspond to changes in climate drivers, such as atmospheric pCO (sub 2) , atmospheric circulation, and glacial-interglacial cycles. 2008-05 Scotese, C.R., Zumberge,J., Illich, H., Moore,T, and Ramos, S., 2008. Using Paleoclimate Models to Predict Source Rock Occurrence: Results from the GANDOLPH Project, American Association of Petroleum Geologists Annual Convention and Exhibition, April 20-23, 2008, San Antonio, Texas, Abstracts Volume, p. 183-184. Abstract: Understanding the temporal and spatial distribution of source rocks, especially in unexplored and under-explored frontier regions is one of the greatest challenges in hydrocarbon system analysis. In order to address this problem, GeoMark Research Ltd, together with the PALEOMAP Project and PaleoTerra Inc., for the past 3 years, have been building a GIS atlas of plate tectonic, paleogeographic and paleoclimatic maps that illustrate the paleoenvironmental setting of known source rocks and oils (GANDOLPH Project). Eight of 12 planned intervals have been completed (mid-Miocene, C/T, Early Cretaceous, Late Jurassic, Late Triassic, Early Permian, Late Devonian, and latest Ordovician-early Silurian). One of the principal research goals of the GANDOLPH Project has been to test the paleoclimatic predictions made by the paleoclimate simulations with information about source rock paleoenviornmental conditions obtained from biomarkers in the oils. A second major research goal of the project has the construction of a tool (Source Rocker) that uses multivariate statistical techniques to 1) identify the kinds of paleoenvironments in which source rocks are likely to have formed, and 2) to estimate the reliability of these source rock predictions. In this talk we will briefly review the results from all eight time intervals, and then discuss, in detail, the results from the C/T (Cenomanian/Turonian) and Late Devonian simulations. We will describe how we built the SourceRocker tool, and will review the predictions it has made regarding the occurrence of probable source rocks in unexplored, and under-explored frontier regions. 2008-06 Peters, K. E., Ramos, L. S., Zumberge, J. E., Zenon V., and, Scotese, C. R., 2008. Restoration of circum-Arctic Upper Jurassic source rock paleolatitude based on crude oil geochemistry, American Association of Petroleum Geologists Annual Convention and Exhibition, April 20-23, 2008, San Antonio, Texas, Abstracts Volume, p. XX Abstract: Tectonic geochemical paleolatitude (TGP) models were developed to predict the paleolatitude of petroleum source rock from the geochemical composition of crude oil. The results validate studies designed to reconstruct ancient source rock depositional environments using oil chemistry and tectonic reconstruction of paleogeography from coordinates of the present day collection site. TGP models can also be used to corroborate tectonic paleolatitude in cases where the predicted paleogeography conflicts with the depositional setting predicted by the oil chemistry, or to predict paleolatitude when the present day collection locality is far removed from the source rock, as might occur due to long distance subsurface migration or transport of tarballs by ocean currents. Biomarker and stable carbon isotope ratios were measured for 496 crude oil samples inferred to originate from Upper Jurassic source rock in West Siberia, the North Sea and offshore Labrador. First, a unique, multi-tiered chemometric (multivariate statistics) decision tree was used to classify these samples into seven oil families and infer the type of organic matter, lithology and depositional environment of each organofacies of source rock [Peters, K.E., Ramos, L.S., Zumberge, J.E., Valin, Z.C., Scotese, C.R., Gautier, D.L., 2007. Circum-Arctic petroleum systems identified using decision-tree chemometrics. American Association of Petroleum Geologists Bulletin 91, 877-913]. Second, present day geographic locations for each sample were used to restore the tectonic paleolatitude of the source rock during Late Jurassic time (approximately 150 Ma). Third, partial least squares regression (PLSR) was used to construct inear TGP models that relate tectonic and geochemical paleolatitude, where the latter is based on 19 source-related biomarker and isotope ratios for each oil family. The TGP models were calibrated using 70% of the samples in each family and the remaining 30% of samples were used for model validation. Positive relationships exist between tectonic and geochemical paleolatitude for each family. Standard error of prediction for geochemical paleolatitude ranges from 0.9 degrees to 2.6 degrees of tectonic paleolatitude, which translates to a relative standard error of prediction in the range 1.5-4.8%. The results suggest that the observed effect of source rock paleolatitude on crude oil composition is caused by (i) stable carbon isotope fractionation during photosynthetic fixation of carbon and (ii) species diversity at different latitudes during Late Jurassic time. 2008-07 Scotese, C.R., 2008. Plate Tectonic and Paleogeographic Mapping: State of the Art, American Association of Petroleum Geologists Annual Convention and Exhibition, April 20-23, 2008, San Antonio, Texas, Abstracts Volume, p. 183. Abstract: How well do we know the configurations of the continents and ocean basins back through time? How accurate are our interpretations of long-eroded mountain ranges and ancient shallow seas? It has been over 40 years since the plate tectonic revolution, what have we learned? How much do we really know? Where should we be focusing our research efforts? Though there have been incremental improvements in our knowledge, the geological and geophysical datasets upon which these reconstructions are based have not changed much in nearly 20 years ago. There are less than a dozen research groups that produce global plate tectonic and paleogeographic reconstructions. Is there general agreement between these groups concerning plate positions and paleogeography through time? How do the interpretations of each of these groups differ? How do we quantify what we know and what we don't know? Though unanswered questions remain, the advent of GIS technology (ArcGIS 9.2 from ESRI) has made it easier to gather the data needed to tackle the remaining questions. Plate tectonic and paleogeographic mapping is now an important tool that is helping the oil industry better understand the formation and development of hydrocarbon systems in frontier areas. Paleogeographic maps are the foundation upon which sophisticated climate models are being run to predict the spatial and temporal distribution of source rocks and reservoir rocks. The newest generation of paleogeographic maps include 3D digital elevation models (PaleoDEMs) that model past changes in bathymetry and topography. This talk will 1) present snap shots from the PaleoAtlas for ArcGIS, a compilation of 50 plate tectonic and paleogeographic reconstructions assembled by the PALEOMAP Project, and 2) will include a 3D computer animation that illustrates plate motions and paleogeographic changes during the last 750 million years. 2008-08 Zumberge, J.E., Scotese, C.R., Moore, T., Illich, and H., Brown, S.W., 2008. Late Devonian Phytoplankton Productivity Enhanced by Aeolian Iron?, American Association of Petroleum Geologists Annual Convention and Exhibition, April 20-23, 2008, San Antonio, Texas, Abstracts Volume, p. 184. Abstract: Frasnian-Famennian organic-rich marine sediments have contributed oil to numerous petroleum systems. In North America, these include the Anadarko Woodford, Illinois New Albany, Michigan Antrim, Appalachian Ohio/Chattanooga, Williston Bakken, and Western Canadian Exshaw and Duvernay. Elsewhere, Frasnian source rocks are well known from the Ghadames, Canning, Timan Pechora, and Volga-Ural basins. The end Frasnian was one of the "big five" global mass extinction events, and was likely caused by extremely high phytoplankton productivity and resulting widespread anoxia. Drawdown of atmospheric CO (sub 2) and resultant global cooling and sea level drop together with the massive burial of organic carbon all contributed to the demise of benthic marine animals. Various mechanisms for supplying abundant nutrients include prevalent upwelling, increased riverine transport of nutrients due to extensive colonization of vascular land plants as well as coeval orogenesis. Recent reports specify that aeolian transport of iron (a necessary nutrient for phytoplankton growth) to the modern Southern and Pacific oceans greatly enhances gross primary productivity downwind of dry continental regions. In our paleogeographic and paleoclimatic modeling of the Late Devonian earth system, we show an extensive equatorial arid belt south and east of the Appalachian/Anadarko basins with strong offshore winds that may have supplied wind-blown iron nutrients for optimal phytoplankton growth. Late Devonian crude oil biomarkers attest to both strong upwelling and environments of intense photic zone euxinia. 2008-09 Kominz, M. A., Browning, J. V., Miller, K. G., Sugarman, P. J., Mizintseva, S., and Scotese, C. R., 2008. Late Cretaceous to Miocene sea-level estimates from the New Jersey and Delaware coastal plain coreholes; an error analysis, Basin Research, v. 20, issue 2, p. 211-226. abs on-line 2008-10 Scotese, C.R., 2008. Paleogeographic maps for 650 Ma,458 Ma, 425 Ma, 390 Ma, 306 Ma, 237 Ma, 65 Ma, 18,000 years ago, Modern, +150 Ma future, +250Ma future (Pangea Proxima) on pages 69 -73, in Koloss de Kontinente by Rudiger Vaas, Bild der Wissenschaft, June, 2008, p. 68-73. 2008-11 Main, D.J., Scotese, C.R., 2008. Polar Crossroads: High Latitude Biogeographic Highways, Geological Society of America 2008 Annual Meeting, October 5-9, 2008, Houston, Texas, Abstracts with Programs, v. 40, issue 6, 144-1, BTH 57, p. 139. 2008-12 Scotese, C.R., and Danforth, A., 2008. The Pre-Rift fit of Africa and South America: Guinea Plateau to Falkland Islands, 7th Houston Geological Society/PESGB International Conference on African Exploration and Production, “Africa: Opportunity from Coast to Coast”, September 8-10, Houston, Texas, Program with Abstracts, p. 2. 2008-13 Moore, T., Scotese, C.R., and Goswami, A., 20008. Predicting Paleosol Distributions Using Paleoclimate Simulations: Results for the Late Devonian, Early Permian, Late Triassic, Late Jurassic, Late Cretaceouis (Cenomanian), and Early Eocene, Geological Society of America Annual Meeting, October 5-9, 2008, Houston, Texas, Abstracts with Programs, v. 40, issue 6, 94-20, BTH 100, p. 259. Abstract: Different kinds of soils form in different climate regimes. For example organic-rich histosols often form in the low-lying, permanently waterlogged landscapes typical of tropical, everwet climates. Aridisols, as the name suggests are found in arid to semi-arid regions. Because soils so closely match climate regimes, they are one of the best indicators of past climates. In this paper we use the associations between modern soil types and modern climate to build a "paleosol prediction program". There are two principal inputs for the paleosol prediction program 1) a present-day, digital map of the world's soil types, and 2) a digital map of global of modern seasonal rainfall and temperature patterns. Using a multivariate approach, the best fit between a given soil type and the range of rainfall and temperature was determined. Each major soil type has a unique climatic "fingerprint" or "climate envelop" defined by a range rainfall and temperature values. In the next step, a paleoclimate simulation using the Fast Ocean and Atmosphere Model (FOAM) was run for six time intervals: the Late Devonian, Early Permian, Late Triassic, Late Jurassic, Late Cretaceous (Cenomanian), and early Eocene. 3D, paleotopographic maps for each of these time intervals was provided by the PALEOMAP Project. Using the climate envelops for each soil type, we were able to map out the predicted paleodistribution of each of these soil types on the paleogeographic maps. It is interesting to note that the extent and relative abundance of these soil types changes through time. The next step in the analysis will be to test the predicted paleosol locations using the database of climatically sensitive rock types compiled by Boucot, Chen and Scotese, and available paleosol information. 2008-14 Scotese, C.R., Bammel, B., Crowley, C., and Versova, L., 2008. Permian and Triassic Plate Tectonic Reconstructions and Animation, Geological Society of America Annual Meeting, Houston, Texas, October 5-9, 2008, Houston, Texas, Abstracts with Programs, 337-7, p.535. 2008-15 Scotese, C.R., Dammrose, R., 2008. Plate Boundary Evolution and Mantle Plume Eruptions during the last Billion Years, Geological Society of America 2008 Annual Meeting, October 5-9, 2008, Houston, Texas, Abstracts with Programs, v. 40, issue 6, Abstract 233-3, p. 328. Abstract: The convective engine that drives the plates is composed of two major components: 1) cold lithospheric slabs sink back into the mantle in subduction zones, and 2) hot material rising from the core mantle boundary in the form a of mantle plumes (hot spots). Plate motions are driven primarily by the negative bouyancy of the subducting slab (slab pull, approximately 70%), the horizontal component of gravity that acts perpendicular to the mid-ocean ridge axes (ridge push, approximately 20%), and the entrainment of the deep roots of the continental lithosphere in the upper mantle (mantle drag, approximately 10%). The motions of the lithosphere, together with initiation of mantle plumes, provides the major boundary conditions that constrain the evolving pattern of convection in the deep Earth. In order to model the pattern of mantle convection during the last 1000 million years, it is necessary to construct a global, plate tectonic model that describes the continuous evolution of plate boundaries and the sporadic occurrence of mantle plumes. In this paper we present an animation that illustrates: 1) the evolution of plate boundaries since the early Neoproterozoic (1200 Ma), and the location and timing of mantle plume eruptions. also animation 2008-16 Shields, C.A., Kiehl, J.T., and Scotese, C.R., 2008. Simulating the Late Ordovician (445 Ma) with the fully coupled Community Climate System Model (CCSM3), American Geophysical Union 2008 Fall Meeting, San Francisco, CA, Eos, Transactions, American Geophysical Union, v.89, issue 53, Abstract PP21B-1432. 2008-17 Scotese, C.R., 2008, in Commission for the Geological Map of the World, 2008. The Geological Map of the World, 3rd edition, 1:25,000,000. (110) (CRS submitted compilation of Mesozoic and Cenozoic ophiolite localities to be included on map.) 2008-18 Scotese, C.R., Illich, H., Zumberge, J, and Brown, S., and Moore, T., 2008. The GANDOLPH Project: Year Two Report: Paleogeographic and Paleoclimatic Controls on Hydrocarbon Source Rock Deposition, A Report on the Methods Employed, the Results of the Paleoclimate Simulations (FOAM), and Oils/Source Rock Compilation, Conclusions at the End of Year Two: Miocene (10Ma), Aptian/Albian (120 Ma), Berriasian/Barremian (140 Ma), Late Triassic (220 Ma), and Early Silurian (430 Ma), July, 2008. GeoMark Research Ltd, Houston, Texas, 177 pp.. 2008-19 Scotese, C.R., 2008, The PALEOMAP Project PaleoAtlas for ArcGIS, version 1, Volume 1, Cenozoic Paleogeographic and Plate Tectonic Reconstructions, PALEOMAP Project, Arlington, Texas. 2008-20 Scotese, C.R., 2008, The PALEOMAP Project PaleoAtlas for ArcGIS, version 1, Volume 2, Cretaceous Paleogeographic and Plate Tectonic Reconstructions, PALEOMAP Project, Arlington, Texas. 2008-21 Scotese, C.R., 2008, The PALEOMAP Project PaleoAtlas for ArcGIS, version 1, Volume 3, Triassic and Jurassic Paleogeographic and Plate Tectonic Reconstructions, PALEOMAP Project, Arlington, Texas. 2008-22 Scotese, C.R., 2008, The PALEOMAP Project PaleoAtlas for ArcGIS, version 1, Volume 4, Late Paleozoic Paleogeographic and Plate Tectonic Reconstructions, PALEOMAP Project, Arlington, Texas. 2008-23 Scotese, C.R., 2008, The PALEOMAP Project PaleoAtlas for ArcGIS, version 1, Volume 5, Early Paleozoic Paleogeographic and Plate Tectonic Reconstructions, PALEOMAP Project, Arlington, Texas. 2008-24 Scotese, C.R., 2008, The PALEOMAP Project PaleoAtlas for ArcGIS, version 1, Volume 6, Late Precambrian Paleogeographic and Plate Tectonic Reconstructions, PALEOMAP Project, Arlington, Texas. 2008-25 Scotese, C.R., 2008. Circum-Arctic Regional Study, Part 1., Plate Tectonic Model for the Arctic Ocean and Its Borderlands: “Windshield Wiper” and “Roll-Back” Tectonics, PALEOMAP Project, Arlington, Texas. “ Geologists of the World, Unite”, an abstract describing the GlobalGeology website that was published in 2006 at the Annual GSA meeing in Philadelphia was reprinted in a 2007 in a computer science journal (I can’t email or name of the journal). (104) 2008_26 Scotese, C. R., 2008. Precambrian paleogeographic map, p. 23; Cambrian paleogeographic map, p. 37; Ordovician paleogeographic map, p. 47; Silurian paleogeographic map, p. 57; Devonian paleogeographic map, p. 65; Carboniferous paleogeographic map, p. 73; Permian paleogeographic map, p. 85; Triassic paleogeographic map, p. 95; Jurassic paleogeographic map, p. 107; Cretaceous paleogeographic map, p. 117; Paleogene paleogeographic map, p. 130; Neogene paleogeographic map, p. 139; Quaternary paleogeographic map, p. 150; in Ogg, J.G., Ogg, G., and Gradtein, F.M., 2008. The Concise Geologic Time Scale, Cambridge University Press, 177 pp. 2009 2009-01 White, J.M., Jessop, C.M., Scotese, C.R., Lai, G., and R.J. da Roza, 2009. Depicting biostratigraphical data from Palynodata: Experiments and questions in data presentation and manipulation, Palynology, v. 33:157-174. (109c) Abstract: Experiments are presented here in analysis and depiction of Palynodata records. Palynodata, a database of pre-Quaternary records of fossil palynomorphs compiled from global literature, is now available as Geological Survey of Canada (GSC) Open File 5793. Palynodata is a non-random sample of the distributions of palynomorphs. Hence, for any taxon, occurrence records in Palynodata serve as a proxy for its "real" distribution in geological time and paleogeographical space. These experiments may be useful starting points for students of palynology in their exploration of Palynodata records. Palynoplot software bins and plots. Palynodata taxa retrievals by time, and by the modern latitude of the study sites. It uses geographical coordinates for the study localities in Palynodata and the geological time scale. Such plots reveal temporal and latitudinal distribution patterns, and potential taxonomic and data problems such as outliers and inconsistent taxonomy. Taxonomic studies can be supported by considering time by latitude distributions, in addition to traditional morphology and priorities. The modern latitude of the sites studied gives increasing distortion with geological age. Palynodata output and the study locality file was input for PaleoGIS software to depict occurrence records on paleogeographical maps. PaleoGIS software showed changing occurrence patterns on rotated plates. An experimental trend surface model of the Jurassic-Cretaceous transition used binned records of common filicale genera which were evolutionarily sensitive between 180 and 100 Ma. The results demonstrate potential for the technique, and lessons for interpretation and future refinement. Common taxa may become useful for biostratigraphical problems and, by calibration against reference sections, this technique might be refined to provide a useful biostratigraphical standard for geological system boundaries. These manipulations of Palynodata records are a "proof-of-concept" demonstration of techniques that may help to reveal the biostratigraphical, paleoecological, and paleoclimatological significance of fossil palynomorphs. Such work also reveals desirable improvements in Palynodata. The precision of indexing species in Palynodata may limit the potential level of chronostratigraphical resolution. 2009-02 Boucot, A.J., Chen Xu, Scotese, C.R., and Fan Jun-Xuan, 2009. Atlas of Phanerozoic Lithologic Indicators of Climate, Science Press, 204 pp. (in Chinese). (108) 2009-03 Jacobs, L.L., Mateus, O., Polcyn, M.J., Schulp, A.S., Scotese, C.R., Goswami, A., Ferguson, K.M., Robbins, J.A., Vineyard, D.P., and A. Buto-Neto, 2009, Cretaceous paleogeography, paleoclimatology, and amniote biogeography of the low and mid-latitude South Atlantic Ocean, Bulletin de la Societe Geologique de France, v. 180:333-341. (106) 2009-04 Scotese, C.R., 2009. Late Proterozoic plate tectonics and paleogeography: A tale of two supercontinents, Rodinia and Pannotia, in Global Neoproterozoic petroleum systems: The emerging potential in North Africa, J. Craig, J. Thurow, A. Whitman, and Y. Abutarruma (editors), Geological Society of London Special Publication 326, pp. 67-83. Abstract: The plate tectonic and palaeogeographic history of the late Proterozoic is a tale of two supercontinents: Rodinia and Pannotia. Rodinia formed during the Grenville Event (c. 1100 Ma) and remained intact until its collision with the Congo continent (800-750 Ma). This collision closed the southern part of the Mozambique Seaway, and triggered the break-up of Rodinia. The Panthalassic Ocean opened as the supercontinent of Rodinia split into a northern half (East Gondwana, Cathaysia and Cimmeria) and a southern half (Laurentia, Amazonia-NW Africa, Baltica, and Siberia). Over the next 150 Ma, North Rodinia rotated counter-clockwise over the North Pole, while South Rodinia rotated clockwise across the South Pole. In the latest Precambrian (650-550 Ma), the three Neoproterozoic continents--North Rodinia, South Rodinia and the Congo continents--collided during the Pan-Africa Event forming the second Neoproterozoic supercontinent, Pannotia (Greater Gondwanaland). Pan-African mountain building and the fall in sea level associated with the assembly of Pannotia may have triggered the extreme Ice House conditions that characterize the middle and late Neoproterozoic. Although the palaeogeographic maps presented here do not prohibit a Snowball Earth, the mapped extent of Neoproterozoic ice sheets favour a bipolar Ice House World with a broad expanse of ocean at the equator. Soon after it was assembled (c. 560 Ma), Pannotia broke apart into the four principal Palaeozoic continents: Laurentia (North America), Baltica (northern Europe), Siberia and Gondwana. The amalgamation and subsequent break-up of Pannotia may have triggered the "Cambrian Explosion". The first economically important accumulations of hydrocarbons are from Neoproterozoic sources. The two major source rocks of this age (Nepa of Siberia and Huqf of Oman) occur in association with massive Neoproterozoic evaporite deposits and in the warm equatorial-subtropical belt, within 30 degrees of the equator. 2009-05 Main, D.J., and C.R. Scotese, 2009. Polar paleobiogeographic pathways: Beringia and Barentsia as dinosaur biogeographic highways, Geological Society of America, South-Central section, 43th annual meeting, abstracts with programs, v. 41:31. Abstract: When Pangea broke apart in the Late Jurassic, widening ocean basins separated land areas in tropical and temperate latitudes. However, at the North and South Poles, land areas remained connected throughout most of the Jurassic, Cretaceous and Cenozoic. In the Northern Hemisphere, terrestrial migration routes can be traced eastwards from Greenland to Europe and northern Asia throughout the Triassic, Jurassic, Cretaceous and through the Cenozoic until the Oligocene. Connections between western North America and northeastern Eurasia, through Beringia, were more sporadic, but a good case can be made that Arctic Canada and Siberia were connected continuously since the Albian (approximately 100 Ma). In the Southern Hemisphere, migration pathways were more complex. South America, Africa, Madagascar, India, Antarctic and Australia were interconnected from the Triassic, throughout the Jurassic and into the Late Cretaceous (approximately 100 Ma). In the late Aptian-early Albian, India and Madagascar became isolated from the other Gondwana continents. India became an island continent shortly thereafter approximately 90 Ma). Migration from South America down the West Antarctic Peninsula, across Antarctica and into Australia was possible until the establishment of the Drake Passage and Tasman-Antarctic strait (approximately 40 Ma). In this paper we will present 15 paleogeographic maps centered on the North South Poles that illustrate the polar biogeographic highways and crossroads that connected the continents during the Jurassic, Cretaceous and Cenozoic. 2009-06 Main, D.J., Noto, C.R., and C.R. Scotese, 2009. Late Jurassic - Early Cretaceous dinosaur paleobiogeography within Northern Hemisphere ecosystems: Beringia and Barentsia, 9th North American Paleontological Convention, v. 9:205. 2009-07 Scotese, C.R., and D.J. Main, 2009. Mesozoic paleogeography and the paleogeographic connectivity index (PCI), 9th North American Paleontological Convention, v. 9:207-208. 2009-08 Upchurch, G. R., Kiehl, J., Shields, C., and C. R. Scotese, 2009. Coupled climate model simulations of the latest Cretaceous (Maastrichtian): Comparison with proxy data, Geological Society of America, 2009 annual meeting, abstracts with programs, v. 41:566-567. 2009-09 Shields, C.A., Kiehl, J.T., Upchurch, G.R., and Scotese, C.R., 2009. Monsoons across epochs: Diagnosing monsoonal circulations across warm, greenhouse climates as simulated by the Community Climate System Model (CCSM3), American Geophysical Union 2010 Fall Meeting, Eos, Transactions, American Geophysical Union, v. 90, Issue 52, Abstract PP41A, p.1481. 2009-10 Upchurch, G.R., Kiehl, J.T., Shields, C.A., and C.R. Scotese, 2009. Coupled climate model simulations of a Late Cretaceous (Maastrichtian) greenhouse climate: Comparison with proxy data, American Geophysical Union 2009 Fall Meeting, Eos, Transactions, American Geophysical Union, v. 90, Issue 52, Abstract PP13B, p.1390. Abstract: Earth's future climate is expected to warm considerably due to increased atmospheric carbon dioxide. Paleoclimate records indicate that pre-Quaternary time periods provide the best possible view of Earth under warm greenhouse conditions. Thus, past warm greenhouse climates provide an important tool to evaluate fully coupled climate models that are currently used to study future climate change. In this study, we use the Community Climate System Model (CCSM3) to investigate the climate of the latest Cretaceous (Maastrichtian). CCSM3 is a fully coupled three-dimensional global model that includes atmospheric, oceanic, sea-ice and terrestrial processes. The CCSM3 simulations employ the paleogeographic and global vegetation reconstructions used in earlier simulations of the late Maastrichtian with the GENESIS Earth System Model (Upchurch, Otto-Bliesner, and Scotese, 1999). CCSM3 simulations include two levels of atmospheric carbon dioxide (2XPAL and 6XPAL), elevated levels of atmospheric methane, changes to low level liquid cloud properties based on the hypothesis of Kump and Pollard (2008), and different paleoelevations for the interior of Siberia. A coupled simulation of multi-century length is carried out to study steady state conditions for the oceans. For terrestrial regions, model mean annual temperatures and seasonality are compared with data from angiosperm leaf physiognomy, plant life form distribution, and other climatic indicators to determine how well the model represents high latitude warmth on a zonal and regional basis. Model precipitation is compared with a database of climatically restricted sediments and angiosperm leaf physiognomy for specific sites. For oceanic regions, the CCSM3 simulations are compared to marine proxies of surface and benthic temperatures to study how well the model captures global Cretaceous ocean circulation patterns. Our results underscore the need for accurate boundary conditions in model simulations and provide a series of baseline simulations for the study of climatic change at the Cretaceous-Paleogene boundary. 2009-11 Goswami, A., Main, D.J., Noto, C.R., Moore, T.L., and Scotese, C.R., 2009. Cretaceous climate sensitivity study using dinosaur and plant paleobiogeography, American Geophysical Union 2009 Fall Meeting, Eos, Transactions, American Geophysical Union, v. 90, Issue 52, Abstract PP31A, p.1358. 2009-12 Scotese, C.R., Illich, H., Zumberge, J, and Brown, S., and Moore, T., 2009. The GANDOLPH Project: Year Three Report: Paleogeographic and Paleoclimatic Controls on Hydrocarbon Source Rock Deposition, A report on the Results of the Paleogeographic, Paleoclimatic Simulations (FOAM), and Oils/Source Rock Compilation, Conclusions at the End of Year Three: Eocene (45Ma), Early/Middle Jurassic (180 Ma), Mississippian (340 Ma), Neoproterozoic (600 Ma), August 2009. GeoMark Research Ltd, Houston, Texas, 154 pp. 2010 2010-01 Winguth, A., Osen, A., Scotese, C.R., and Winguth, C., 2010. Changes of the Late Permian Ocean Circulation and Seep-Sea Anoxia in Response to Tectonic Changes - A Model Study with CCSM3, AAPG Annual Convention and Exposition, New Orleans, LA, April 11-14, 2010 (abstract). 2010-02 Jacobs, B.F., Pan, A.D., and C. R. Scotese, 2010. A review of the Cenozoic vegetation of Africa, in Cenozoic Mammals of Africa, Werdelin, L., and Sanders, W.J., (editors), University of California Press, Berkeley, CA, p. 57-72. (105) Abstract: The aim of this chapter is to review and interpret the Cenozoic paleobotanical record of Africa. Ideally, we want to present a dynamic view of plant community and ecosystem change through time, so that the evolutionary and biogeographic history of Cenozoic African mammals can be considered in the context of the communities to which they belonged. To facilitate this goal, we discuss environmental change in the context of major physiographic change such as graben formation associated with rifting in East Africa, and show paleobotanical sites in their correct position on paleogeographic maps (citations provided in table 5.1). However, spatial and temporal coverage are uneven, allowing detailed paleoenvironmental reconstruction for some localities and only the most general inferences for most time intervals. 2010-03 Chatterjee, S., Scotese, C.R., and Bandyopadhyay, S., 2010. The wandering Indian Plate and its changing biogeography during the Late Cretaceous - Early Tertiary Period, Chapter 7., in New Aspects of Mesozoic Biodiversity, Lecture Notes in Earth Sciences 132, Springer-Verlag, Berlin Heidelberg, pp. 105-126. (111) Abstract: he biogeography of Indian tetrapods during the Late Cretaceous-Early Tertiary period provides an unparalleled opportunity to examine the complex ways in which the tetrapods responded to the sequence and timing of the rifting, drifting, and collision of Indian plate. Triassic and Jurassic tetrapods of India have widespread Gondwanan relationships (Chatterjee and Scotese, 1999, 2007). With the breakup of Gondwana, India remained isolated as an island continent, but reestablished its biotic links with Africa, Madagascar, South America, and Asia during the Late Cretaceous (Sahni and Bajpai, 1988; Chatterjee and Scotese, 1999; Khosla and Sahni, 2003). During the Palaeocene, India drifted northward as an island continent, when the tetrapods of Gondwanan heritage presumably evolved in intermittent isolation for 20 Ma and radiated into extraordinary diversity. Endemism ended when the Indian plate collided with Asia at the Palaeocene/Eocene boundary. A northeast migration corridor arose at a time when several groups of newly evolved tetrapods might have dispersed into Asia. India also received many groups of tetrapods from the north during its union with Asia (Russell and Zhai, 1987). A great faunal interchange took place during the Eocene. In this paper we integrate the tectonic evolution of the Indian plate with its biogeography during its long northward journey to test the models of vicariance and geodispersal. 2010-04 Main, D.J., Noto, C.R., and C.R. Scotese, 2010. Coastal Cretaceous forest fires, paleosols, and dinosaur paleoecology from the Arlington Archosaur Site, north Texas, Geological Society of America, 2010 annual meeting, abstracts with programs, v. 42:175. Abstract: This is the first reported occurrence of wildfires from the Cenomanian of Texas at the Arlington Archosaur Site (AAS). The AAS is a diverse fossil locality from the Cretaceous (95 Mya) Woodbine Formation of north Central Texas. The paleoenvironmental setting is a coastal, delta plain system from the southeastern interior seaway. The site preserves multiple components of a delta plain ecosystem within a 2m section consisting of a peat bed containing numerous, well preserved fossil turtle, crocodile (adult and juvenile) and logs. The logs are carbonized and vary from 2m-4m in length. Overlying the peat is a fossil horizon containing mixed remains of vertebrates in a mudstone that demonstrates early pedogenesis from an inundated delta plain paleosol. The vertebrates occurring within this horizon include dinosaur, crocodile, turtle and lungfish. The dinosaurs recovered to date include a large herbivorous ornithopod and at least two theropods. Overlying the fossil bearing horizon is a well developed, heavily rooted Histic Gleysol with numerous calcareous concretions. Within the concretions occur charcoal fragments and several large (28-36 cm length) burned tree stumps and roots. Concretion formation is indicative of seasonal dryness, and the burned tree stumps are evidence of wildfires. Charcoal conglomerate beds were mapped both below and above the paleosol, and dinosaur bone bearing horizon. The charcoal conglomerates contain numerous charcoal and fossil wood fragments (1-4cm length) bound in a Fe rich sand. The presence of charcoal conglomerates is typical of coastal, deltaic systems where burned materials were transported by river channels. The forest fire horizons occur below, within and above the vertebrate fossil horizon. Periodic forest fires are therefore thought to have been an influential part of the coastal ecosystem preserved at the Arlington Archosaur Site. Forest fires are not geographically random, they occur within paleoclimatic zones that are predisposed to fires. Continued study of forest fires may elucidate links between paleoclimate and the biodiversity of coastal Cretaceous ecosystems. 2010-05 Noto, C.R., Main, D.J., Moore, T., Scotese, C.R., and A. Goswami, 2010. Untangling the relationship between climate and biodiversity in Mesozoic terrestrial vertebrates, Geological Society of America, 2010 annual meeting, abstracts with programs, v.42:173-174. Abstract: In the modern world, the relationship between climatic variation and biodiversity is well known and appreciated. Current climatic conditions maintain a unimodal biodiversity gradient that peaks around the equator, decreasing with increasing latitude. This pattern is observed in various groups of plants, vertebrates, and insects as well as in terrestrial, freshwater, and marine environments. The modern biodiversity gradient is assumed to be ancient, stretching back at least 65 my or more. However, prior to the recent icehouse there were several hothouse intervals in Earth's history in which the temperature gradient was more relaxed, leading to climatic conditions unseen in many modern ecosystems. It may therefore be unrealistic to expect the distribution of biodiversity to have remained static during these intervals. In fact, studying past distribution patterns may prove vital to understanding the relationship between climatic variables and current species diversity. Here we present part of an ongoing study into Mesozoic climates and terrestrial vertebrate distribution patterns in which we explore the relationship between body fossils and climate simulations. Fossil distribution data comes from the Paleobiology Database while abiotic parameters (temperature, precipitation, etc.) are derived from Fast Ocean Atmospheric Model (FOAM) simulations for 220, 195, 155, 120, 90, and 70 mya. Throughout much of the Mesozoic, terrestrial vertebrate diversity (especially dinosaurs) appears to follow a bimodal distribution pattern. Likewise, the climate during this time was characterized by strong continentality and a relaxed temperature gradient. The bimodal pattern weakens as continentalality breaks down with Pangean disassembly during the Cretaceous. This suggests that strongly seasonal environments played an important role in supporting biodiversity during the Mesozoic, lending important insights into the ecology of terrestrial ecosystems during this time. Changes in taxonomic diversity over time may also be related then to the expansion or contraction of certain key climate zones and have implications for understanding extinction patterns. Although much work remains to be done, this method presents a promising way for exploring the connection between Earth's climate and biota. 2010-06 Stolz, A. and Scotese, C.R., 2010. The evolution of river systems during the breakup of Pangea (240 - 80 mya), Geological Society of America, 2010 annual meeting, abstracts with programs, v. 42:242. Abstract: Digital elevation models (paleoDEMs) were constructed for five intervals during the Mesozoic: Triassic (240 Ma), Jurassic (200 Ma and 160 Ma), and Cretaceous (120 Ma and 80 Ma). The Hydrology tools (ArcGIS, ESRI) were then used to map the paleodrainage patterns and the location of ancient river systems for five time intervals. During this period of Earth History the supercontinent of Pangea, which occupied over 40% of Earth's surface, rifted apart to form the modern continents and ocean basins. A statistical analysis was performed to characterize the average length of river systems and the average area of drainage basins before, during and after breakup of Pangea. As expected, the average length of rivers and the average area of drainage basins decreased as consequence of continental fragmentation. However, other variables turned out to be equally, or more important. River length and drainage area were also affected by: changes in global sealevel, mountainbuilding, and the changing location of land areas with respect to the Equatorial Rainy Belt and Subtropical Arid Belt. 2010-07 Winguth, A., Osen, A., Scotese, C.R., and C. Winguth, 2010. Paleogeography of the Late Permian: Implications for climate, geochemical cycles, and mass extinction, Geological Society of America, 2010 annual meeting, abstracts with programs, v. 42:71. Abstract: By the end of the Late Permian, most continents had collided to form the supercontinent of Pangea, a concept originally proposed by Alfred Wegener. The general geographic settings for this time are well-known, but the positions of Panthalassic mid- ocean ridges and of Tethian islands and seaways and their impact on the environment are uncertain. The geographic and tectonic changes at the Permian-Triassic boundary affected significantly the most severe mass extinction of species. One hypothesis for the extinction favors a climatic response to an increase in tectonic activity and associated l large-scale volcanism, resulting in ocean stagnation and widespread anoxia with fatal consequences for marine and land organism. The concept is supported by recent interpretations of geochemical data suggesting that periodic upwelling of toxic hydrogen sulfide-rich water masses contributed to the extinction of species. In this paper, we review the impact of mid-ocean ridges and sill depths on the Late Permian climate and the implications for widespread anoxia and extinction. Comprehensive climate model results indicate that ridges promote diapycnal mixing along the ridge axis, but enhance inter-basin gradients of oxygen. Shallow passages between the Tethys and Panthalassa could have contributed to stagnation and low oxygen concentrations in the Tethyan basin. The climatic changes and tectonic activities at the end of the Permian, enhancing continental weathering and thus increasing nutrient input into the ocean, may have drastically changed marine productivity patterns and hence oxygen consumption in the deep sea. 2010-08 Scotese, C.R., 2010. The PALEOMAP PaleoAtlas (ArcGIS), Geological Society of America, 2010 annual meeting, abstracts with programs, v. 42:457. Abstract: During the last six years the PALEOMAP Project has constructed a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions. This "PaleoAtlas" runs in ArcGIS (ESRI) and takes full advantage of the cartographic and database functionality of this GIS (Geographic Information System). The PaleoAtlas is made up of six volumes: Cenozoic, Cretaceous, Jurassic and Triassic, late Paleozoic, early Paleozoic, and late Precambrian (Neoproterozoic). Each volume has 8-10 paleoreconstructions; there are 53 paleoreconstructions reconstructions in the completed PaleoAtlas. The oldest paleoreconstruction dates from the breakup of Rodinia (750 Ma, Cryogenian). For each reconstructed time interval there are more than 25 feature layers (map overlays) that describe important tectonic, paleogeographic and paleoclimatic information such as: modern geographic features (political boundaries, coastlines, cities, river and lakes), plate tectonic features (active plate boundaries, age of the ocean floor, ancient plates, and vectors describing plate motion), paleorivers and drainage basins, paleoclimatic information (lithologic indicators of climate such as coals, evaporites, calcretes, tillites, etc), ancient climate zones (Equatorial Rainy Belt, Arid Belt, Warm and Cool Temperate, Polar ), a 3D digital paleogeographic model (PaleoDEM), as well as estimates of highstand and lowstand shorelines, and geological information (outcrop geology, regional lithofacies, coral reefs, and ophiolites) The spatial-temporal framework provided by the PALEOMAP PaleoAtlas is the foundation for the "Earth System History Archive" (ESHA). The Earth System History Archive, in collaboration with the Paleobiology Database, the Global Geology website, and the Paleoclimate Atlas, is a compilation of important paleo-environmental variables (e.g., elevation, bathymetry, temperature, rainfall, ocean currents, salinity, upwelling, etc.). The goal of the Earth System History Archive is to provide earth scientists and earth historians with a concise, accurate, and informative digital description of the evolution of the Earth System during the past one billion years. Using GIS technology it is now possible to store, retrieve and visualize this wealth of information about the Earth's distant past. 2010-09 Yamusah, A., Scotese, C.R., Goswami, A. and T.L. Moore, 2010. Predicting the occurrence of evaporites using climate modeling (FOAM), Geological Society of America, 2010 annual meeting, abstracts with programs, v. 42:598-599. Abstract: Evaporites form under specific climatic conditions. Though the factors that control evaporite formation may complex (Peryt, 1987), the two principal variables are the mean annual temperature (MAT) and the annual amount of precipitation. Because modern evaporites have a limited extent, we have chosen to use the Yermosol-Solonchak soil type (Zobler, 1886) as a proxy for the conditions under which evaporites form and have constructed a model that predicts the likelihood that evaporites would form under varying temperature and precipitation conditions. Our results suggest that areas with mean annual temperatures between 21 degrees C and 24 degrees C, and average annual rainfall of less than 1 mm/month would be the mostly likely sites of evaporite formation. From this bivariate description of evaporite formation, we have constructed a "climate envelope" that predicts the likelihood of evaporite formation. The climate envelop model can then be tested by comparing the predictions made by our model with the distribution of ancient evaporites (Boucot et al., in press). Predictions of the global occurrence of evaporites have been made for 18 time intervals during the Phanerozoic and late Precambrian: late Miocene (10 ma), Oligocene (30 Ma), late Eocene (45 Ma), K/T boundary (65 Ma), Cenomanian/Turonian(90 Ma), early Aptian (120 Ma), earliest Cretaceous (140 Ma), Late Jurassic (160 Ma), Early Jurassic (180 Ma), Late Triassic (220 Ma), Permo-Triassic (250 Ma), Early Permian (280 Ma), Mississippian (340 Ma), Late Devonian (360 Ma), Siluro-Devonian (400 Ma), latest Ordovician (430 Ma), Cambro-Ordovician (480 MA), and late Neoproterozoic (600 Ma). These predictions of evaporite occurrence are based on the estimates temperature and precipitation made by the FOAM (Fast Ocean and Atmosphere Model) climate model in combination with the paleogeographic maps produced by the PALEOMAP Project. We will present paleoreconstructions comparing the predicted occurrence of evaporites since the late Proterozoic with the known distribution of ancient evaporites. 2010-10 Moore, T.L., and C.R. Scotese, 2010. The Paleoclimate Atlas (ArcGIS), Geological Society of America, 2010 annual meeting, abstracts with programs, 42:598. Abstract: Work has begun on a Paleoclimate Atlas that uses the Fast Ocean and Atmosphere Model (FOAM) and GIS software (ArcGIS, ESRI) to illustrate the Earth's evolving climate during the past 750 million years. The Paleoclimate Atlas is made up of four volumes: 1) Cenozoic, 2) Cretaceous and Late Jurassic, 3) late Paleozoic and early Mesozoic (Carboniferous-Early/Middle Jurassic), and 4) late Precambrian and early Paleozoic. There will be more than 50 paleoclimatic reconstructions in the completed Paleoclimate Atlas. As of June 2010, 18 simulations have been run: late Miocene (10 ma), Oligocene (30 Ma), late Eocene (45 Ma), K/T boundary (65 Ma), Cenomanian/Turonian(90 Ma), early Aptian (120 Ma), earliest Cretaceous (140 Ma), Late Jurassic (160 Ma), Early Jurassic (180 Ma), Late Triassic (220 Ma), Permo-Triassic (250 Ma), Early Permian (280 Ma), Mississippian (340 Ma), Late Devonian (360 Ma), Siluro-Devonian (400 Ma), latest Ordovician (430 Ma), Cambro-Ordovician (480 Ma), and Neoproterozoic (Snow Ball Earth, 600 Ma). For each paleoclimatic reconstruction, there are approximately 20 feature layers describing important aspects of the Earth's ancient climate: atmospheric circulation (seasonal pressure systems and winds), seasonal temperatures, rainfall, runoff, paleorivers and drainage basins, oceanography (seasonal surface currents, salinity, areas of upwelling, areas of anoxia), and paleogeography (highstand and lowstand coastlines, a 3D digital elevation model, and the predicted location of deltas and clastics influx to the oceans). The climatic information collected in the PaleoclimateAtlas will be a principal input for the "Earth System History Archive" (ESHA). The Earth System History Archive, in collaboration with the Paleobiology Database, the Global Geology website, and the PALEOMAP PaleoAtlas, is a compilation of important paleo-environmental variables (e.g., elevation, bathymetry, temperature, rainfall, ocean currents, salinity, upwelling, etc.). The goal of the ESHA is to provide earth scientists and Earth historians with a concise, accurate, and informative digital description of the evolution of the Earth System during the past one billion years. Using GIS technology it is now possible to store, retrieve, and visualize this wealth of information about the Earth's distant past. 2010-11 Jabri, N., Scotese, C.R., and D.J. Main, 2010. Dinosaur biogeography: migration pathways and refugia, Geological Society of America, 2010 annual meeting, abstracts with programs, v. 42:249. Abstract: Dinosaurs were terrestrial travelers. They did not travel by air or sea, only by land relying on "landbridges" to connect them to distant places. Land-bridges, in turn, were controlled by mountain building events (on timescales of 10's of my), plate tectonic events like continental rifting and collision (also on timescales of 10's of my), and changes in sea-level (eustatic events, 100,000's yrs). The most important factor controlling dinosaur migration pathways was eustatic events. "Connectivity" between distant places was high during lowstands (when sea level may have fallen to the edge of the continental shelves) and low during highstands (when sea level may have been 200-300 meters higher than today). During sea level highstands dinosaurs were isolated on numerous "continental island refugia". There were two types:continental island refugia: "temporary or highstand" refugia which were reconnected during lowstands of sealevel (e.g. eastern and western North America), and "permanent or island" refugia which were isolated during times of high and low sealevel (e.g., Madagascar). Evolutionary exchanges regularly occurred between temporary refugia. Evolutonary exchanges rarely occurred between permanent refugia. "Paleogeographic connectivity" is defined as geographic distance between the geographic centroids of each highstand refugia. The faunal similarity between two highstand refugia will be a function of the paleogeographic connectivity (and other factors such as paleoclimatic barriers). Using paleo-digital elevation models from the PALEOMAP PaleoAtlas and estimates of sealevel change from Haq (1987), highstand refugia were mapped for four intervals during the Cretaceous (Maastrichtian, Cenomanian/Turonian, early Aptian, and Berriasian). Using the ArcGIS tool, Spatial Analyst, "cost weighted distance maps" and "least cost migration paths" were constructed that illustrated the mostly likely paths of dinosaur migration between these temporary refugia. The number of dinosaur migration pathways (DMP) between the temporary refugia was calculated to be, DMP = (n2 -n)/2, where n is the number of temporary refugia. It was noted that some of the dinosaur migration pathways predicted by this analysis correspond to known dinosaur trackways (e.g. North Slope of Alaska). 2010-12 Goswami, A., Scotese, C.R., and Moore, T.L., 2010. Predicting the occurrence of paleosoils using climate modeling (FOAM), Geological Society of America, 2010 annual meeting, abstracts with programs, v. 42:598. Abstract: Because soils form under ambient climatic conditions, they are one of the best indicators of past climates. Though the factors that control soil formation are complex (Retallack, 1990), the two principal variables that determine soil type are mean annual temperature (MAT) and annual amount of precipitation. Seasonal variation in temperature and precipitation is also important. There are several modern soil classification schemes. We have chosen the scheme proposed by Zobler (1986) which is based on the FAOUNESCO (1974) soil classification scheme. We have constructed a model that predicts the kind of soil that would be expected to form under varying temperature and precipitation conditions. For example areas with mean annual temperatures between 21 degrees C and 24 degrees C, and average annual rainfall of less than 1 mm/month, would most like have a Yermosol-Solonchak soil type. Whereas, Ferralsol-Nitosol type soils are predicted to develop in areas with mean annual temperatures between 22 degrees C and 26 degrees C, and average annual rainfall between 12-25 mm/month. Using this bivariate description of soil types we have constructed "climate envelops" that characterize 10 modern soil types (Acrisol, Cambisol-Gleysol, Chernozem- Podzoluvisol-Greyzem, Ferralsol-Nitosol, Phaeozem, Kastanozem-Solonetz, Histosol-Podzol, Planosol, Vertisol and Yermosol-Solonchak). Because the climatic envelop technique (Moore, 2001) accurately predicts the distribution of modern soils, we are confident that it can be used to predict the paleogeographic distribution of ancient soil types. These predictions can be tested by comparing the predictions made by our model with the distribution of paleosols (e.g., calcisol, gypsisol, gleysol, argillisol, protosol) and other lithologic indicators of climate such as coals, evaporites, bauxites, calcretes, etc.. Predictions of the paleogeographic occurrence of paleosoils have been made for 14 time intervals during the Phanerozoic: late Miocene, Oligocene, late Eocene, K/T boundary, Cenomanian/Turonian, early Aptian, earliest Cretaceous, Late Jurassic, Early Jurassic, Late Triassic, Permo-Triassic, Early Permian, Mississippian, and Late Devonian. We will present paleoreconstructions showing the predicted distribution of paleosoils since the Late Devonian. 2010-13 Shields, C.A., Upchurch, G. R., Kiehl, J.T., Scherer, J., and Scotese, C.R., 2010. Simulating the Warm Arctic Environment for the Latest Cretaceous Using the Community Climate System Model (CCSM3), American Geophysical Union 2010 Fall Meeting, Eos, Transactions, American Geophysical Union, v. XX, Issue XX, Abstract XXXX, p.XXXX. 2010-14 Osen, A., Scotese, C., Winguth, A.M., and Winguth, C., 2010. Sensitivity of Late Permian climate to topographic changes and implications for mass extinctions, American Geophysical Union 2010 Fall Meeting, Eos, Transactions, American Geophysical Union, v. XX, Issue XX, Abstract XXXX, p.XXXX. 2010-15 Jacobs, L.L., Polcyn, M.J., Mateus, O., Schulp, A., Ferguson, K., Scotese, C.R., Jacobs, B.F., Strganac, C., Vineyard, D., Myers, T.S., and Morais, M.L., Tectonic Drift, Climate, and Paleoenvironment of Angola since the Cretaceous, American Geophysical Union 2010 Fall Meeting, Eos, Transactions, American Geophysical Union, v. XX, Issue XX, Abstract XXXX, p.XXXX. Africa is the only continent that now straddles arid zones located beneath the descending limbs of both the northern and southern Hadley cells, and it has done so since it became a distinct continent in the Early Cretaceous. Since that time, Africa has drifted tectonically some 12 degrees north and rotated approximately 45 degrees counterclockwise. This changing latitudinal setting and position of the landmass under the relatively stable Hadley Cells is manifested as southward migration of climatic zones over the past 132 million years. Data from kerogen, X-ray diffraction analysis of sedimentary matrix, carbon isotopes from shell samples and tooth enamel,new 40Ar/39Ar radiometric dates, pollen and plant macrofossils, and fossil vertebrates indicate a productive upwelling system adjacent to a coastal desert since the opening of the South Atlantic Ocean; however, the position of the coastal desert has migrated southward as Africa drifted north, resulting in today's Skeleton Coast and Benguela Current. This migration has had a profound effect on the placement of the West African coast relative to areas of high marine productivity and resulting extensive hydrocarbon deposits, on the placement of arid zones relative to the continent especially the Skeleton Coast desert, on the climatic history of the Congo Basin (which shows a Late Cretaceous decrease in aridity based on the relative abundance of analcime in the Samba core), and in reducing the southern temperate region of Africa from 17% of continental area during the Cretaceous to 2% today. We show here that these related geographic and environmental changes drove ecological and evolutionary adjustments in southern African floras and faunas, specifically with respect to the distribution of anthropoid primates, the occurrence of modern relicts such as the gnetalean Welwitschia mirabilis, endemism as in the case of ice plants, and mammalian adaption to an open environment as in springhares. Africa's tectonic drift through climate zones has been a first-order environmental determinant since the Early Cretaceous. 2010-16 Parfenov, L.M., Berzin, N.A., Badarch, G., Gombosuren, V.G., Bulgatov, A.N., Dril, S.I., Khanchuk, A.I., Kirillova, G.L., Kuz’min, Nokleberg, W.J., M.I., Ogasawara, M., Obolenskiy, A.A., Prokopiev A.V., Rodionov, S.M., Scotese, C.R., TimofeevV.I., Tomurtogoo, O., and Yan Hongquan, 2010. Tectonic and metallogenic model for Northeast Asia, in W.J. Nokleberg, (editor), Metallogenesis and tectonics of northeast Asia: U.S. Geological Survey Professional Paper 1765, chapter 9, 56 p. [http://pubs.usgs.gov/pp/1765/chapter_9/]. 2010-17 Scotese, C.R., 2010. Early Cretaceous paleogeographic map (figure 4), and reconstructions of magnetic data from South Atlantic (figures 5 and 6), and early Cretaceous paleoclimatic reconstruction (figure 7) in, Lentini, M.R., Fraser, S.I., Sumner, H.S., and Davies, R.J., 2010. Geodynamics of the central South Atlantic conjugate margins: implications for hydrocarbon potential, Petroleum Geoscience, volume 16, p. 217-229. DOI 10.1144/1354-079309-909 2011 2011-01 Jacobs, L.L., Strganac, C., and C.R. Scotese, 2011. Plate motions, Gondwana dinosaurs, Noah’s arks, beached Viking funeral ships, ghost ships, and landspans, Anals da Academia Brasileira de Ciencias. v. 83:3-22. (112) Abstract: Gondwana landmasses have served as large-scale biogeographic Noah's Arks and Beached Viking Funeral Ships, as defined by McKenna. The latitudinal trajectories of selected Gondwana dinosaur localities were traced through time in order to evaluate their movement through climate zones relative to those in which they originally formed. The dispersal of fauna during the breakup of Gondwana may have been facilitated by the presence of offshelf islands forming landspans (sensu Iturralde-Vinent and MacPhee) in the Equatorial Atlantic Gateway and elsewhere. 2011-02 Scotese, C.R., 2011. Paleogeographic Reconstructions of the Circum-Arctic Region since the Late Jurassic, AAPG 2011Annual Convention and Exposition, Houston, TX, April 10-13, 2011, (abstract) Search and Discovery Article #30192 (2011) . found abs ppt 2011-03 Scotese, C.R., 2011. Paleogeographic and Paleoclimatic Atlas, AAPG 2011Annual Convention and Exposition, Houston, TX, April 10-13, 2011, (abstract), Search and Discovery Article #30193 (2011). During the last six years the PALEOMAP Project has constructed a digital atlas of plate tectonic and paleogeographic reconstructions. This "PaleoAtlas" runs in ArcGiS (ESRI). The PaleoAtlas is made up of 53 paleoreconstructions in six , volumes: Cenozoic, Cretaceous, Jurassic and Triassic, Late Paleozoic, Early Paleozoic, and Late Precambrian (Neoproterozoic). For each reconstructed time interval there are more than 25 feature layers that describe important tectonic, paleogeographic and paleoclimatic information such as: modern geographic features, plate tectonic features (active plate boundaries, age of ocean floor, and ancient plates), paleorivers and drainage basins, a 3D digital paleogeographic model (PaleoDEM), as well as estimates of highstand and lowstand shorelines, and geological information (outcrop geology, regional lithofacies, coral reefs, and ophiolites). Work has recently begun on a companion PaleoClimate Atlas. Climate simulations were run using the Fast Ocean and Atmosphere Model (FOAM) which illustrate the Earth's evolving climate during the past 750 million years. There will be more than 50 paleoclimatic reconstructions in the completed Paleoclimate Atlas. As of June 2010, 18 simulations have been run. For each paleoclimatic reconstruction, there are ~20 feature layers describing important aspects of the Earth's ancient climate: atmospheric circulation (seasonal pressure systems and winds), seasonal temperatures, rainfall, runoff, paleorivers and drainage basins, oceanography (seasonal surface currents, salinity, areas of upwelling, areas of anoxia), and the predicted location of deltas and clastic influx to the oceans). The plate tectonic, paleogeographic and climatic information collected in the PaleoAtlas and Paleoclimate Atlas will be the principle input for the "Earth System History Archive" (ESHA). The Earth System Archive is a compilation of important paleo-environmental variables (e.g., elevation, bathymetry, temperature, rainfall, ocean currents, salinity, upwelling, etc). The goal of the Earth System Archive is to provide earth scientists and earth historians with a concise, accurate, and informative digital description of the evolution of the Earth System during the past one billion years. Using GIS it is now possible to store, retrieve, and visualize this wealth of information about the Earth’s distant past. 2011-04 Chatterjee, S., Goswami, A., and Scotese, C.R., 2011. Tectonic evolution and paleoclimatic conditions of the Indian Plate during its longest journey, 14th International Gondwana Symposium, “Reuniting Gondwana: the East meets the West”, abstracts, v. 14, p. 13. Abstract: The tectonic evolution of Indian Plate, which started in Early Jurassic ( approximately 180 Ma) with the separation of Gondwana from Laurasia, provides an excellent and complex case history against which various models of plate tectonics like continental breakup, sea-floor spreading, birth of ocean, flood basalt volcanism, hotspot trails, transform faults, subduction, obduction, continental collision, accretion, and mountain building can be tested. A series of plate tectonic maps are presented here illustrating the repeated rifting and morphing of the Indian Platfrom its Gondwana home, its northward journey, its collision first with the Kohistan-Ladakh Arc its NW corner, and then with Tibet at the Indus-Tsangpo Suture, its final accretion to Asia, and the rise of Himalaya and Tibet Plateau by crustal shortening. The relationships between flood basalts and the recurrent consequential breakup of Indian plate from Gondwana are reviewed and a mixed scenario of "active/passive" rifting model is presented. The break up Gondwana and the opening of the Indian Ocean is thought to have been caused by heating of the lithosphere from below by the large Bouvet Plume, whose relicts are short- lasting swarm of plumes including Rajmahal-Kerguelen, Marion, Somnath, and Deccan- Reunion; and a 4,500 Km long hotspot trail along the Ninety East Ridge. On the other hand, plate-boundary forces mediated the collision of Kohistan-Ladakh Arc with present day Indian Plate in the northwest, and the closure of the Neotethys, resulting the northward motion of the Indian Plate since the Late Cretaceous. The obduction at Kohistan-Ladakh Arc might have triggered the acceleration of the Indian Plate (18- 20 cm/yr) from Late Cretaceous ( approximately 85 Ma) to Paleocene ( approximately 55 Ma) and then slowed down to (5 cm/yr) after the continental Indian Plate collided with continental Asia in early Eocene ( approximately 50 Ma). 2011-05 Main, D.J., Noto, C.R., and C.R. Scotese, 2011. Paleoecology of a Cretaceous coastal ecosystem: archosaurs that lived with forest fires, and example from the Woodbine formation, north Texas, Geological Society of America, South-Central section, 45th annual meeting, abstracts with programs, v. 43:7. Abstract: The Arlington Archosaur Site (AAS) is a diverse fossil locality from the Cretaceous (95 Mya) Woodbine Formation of North Central Texas. The paleoenvironment is a coastal, delta plain system from the southeastern interior seaway. The site preserves components of a coastal ecosystem within a 2 m section consisting of a peat bed containing numerous, well preserved fossil turtle, crocodile (adult and juvenile), dinosaur and logs. Overlying the peat is a fossil horizon containing remains of vertebrates in a mudstone that demonstrates early pedogenesis from an inundated delta plain paleosol. The vertebrates occurring within this horizon include dinosaur (ornithopod), crocodile, turtle and lungfish. The dinosaurs recovered to date include a large herbivorous ornithopod and at least two theropods. All of these animals lived along a coastal plain that was beset with wildfires. The AAS preserves a uniquely excellent record of wildfires from the Cenomanian represented by three distinct forest fire (FF) beds. The first FF bed is a charcoal conglomerate that lies beneath the primary vertebrate bearing fossil horizon. The charcoal conglomerate contains numerous charcoal and fossil wood fragments (1-4 cm length) bound in a Fe rich sand. The 2 (super nd) FF bed occurs in a paleosol bed, within concretions that contain charcoal f ragments and several large burned tree stumps and roots. Concretion formation is indicative of seasonal dryness, and the burned stumps are evidence of wildfires. FF bed 3 occurs in mid-section above FF bed 2 and is interpreted as a debris flow, as it is a sand rich charcoal bed with mixed conglomeratic interclasts. The FF horizons occur below, within and above the vertebrate fossil horizons. Periodic forest fires are therefore thought to have been an influential part of the AAS coastal ecosystem. 2011-06 Chatterjee, S., Goswami, A., and C. R. Scotese, 2011. The longest journey: Mantle plume, continental rifting, collision tectonics, and the evolution of the Indian plate, Geological Society of America, 2011 annual meeting, abstracts with programs, v. 43:143. The tectonic evolution of Indian plate, which started in Early Jurassic (-180 Ma) with the separation of Gondwana from Laurasia, provides an excellent and complex case history against which various models of plate tectonics like continental breakup, sea-floor spreading, birth of ocean, flood basalt volcanism, hotspot trails, transform faults, subduction, obduction, continental collision, accretion, and mountain building can be tested. A series of plate tectonic maps are presented here illustrating the repeated rifting and morphing of the Indian plate from its Gondwana home, its northward journey, its collision first with the Kohistan-Ladakh arc in its NW corner, and then with Tibet at the Indus-Tsangpo Suture, its final accretion to Asia, and the rise of Himalaya and Tibet plateau by crustal shortening. The relationships between flood basalts and the recurrent consequential breakup of Indian plate from Gondwana are reviewed and a mixed scenario of 'active/passive’ rifting model is presented. The break up Gondwana and the opening of the Indian Ocean is thought to have been caused by heating of the lithosphere from below by the large Bouvet plume, whose relicts are short-lasting swarm of pluses including Rajmahal-Kerguelen, Marion, Somnath, and Deccan-Reunion; and a 4,500 Km long hotspot trail along the Ninety East Ridge. On the other hand, plate-boundary forces mediated the collision of Kohistan-Ladakh arc with present day Indian plate in the north-west, and the closure of the Neotethys, resulting the northward motion of the Indian plate since the Late Cretaceous. The obduction at Kohistan-Ladakh arc might have triggered the acceleration of the Indian plate (18-20 cm/yr) from Late Cretaceous (~85 Ma) to Paleocene (~55 Ma) and then slowed down to (5 cm/yr) after the continental Indian plate collided with continental Asia in Early Eocene (~50 Ma). 2011-07 Osen, A., Winguth, A., Winguth, C., and C.R. Scotese, Climate sensitivity to topographic changes during the Late Permian and implications for mass extinctions, Geological Society of America, 2011 annual meeting, abstracts with programs, v. 43:507. Abstract: Evidence from stratigraphic sections of the Panthalassa, Paleo- and Neo-Tethys, suggests that oceans incurred wide spread anoxia during the Late Permian that likely contributed to the extinction of more than 90% of marine species. A carbon isotope shift indicates significant perturbations in the carbon cycle occurred during the Late Permian and persisted into the Early Triassic. Bathymetric features of the Panthalassic Ocean are not well known since the ocean floor from 252 Ma has been subducted. Tectonic reconstructions indicate that subduction zones were active along the borders of Pangaea, thus requiring an active ridge or rift system. Most climate simulations have assumed a flat bottom ocean, because the exact location of a mid ocean ridge was uncertain. In this study, two different bathymetric configurations are being considered in the comprehensive climate simulation model (CCSM-3): a ridge simulation where a mid-ocean ridge was placed within the Panthalassa Ocean and a simulation in which the deep Tethys Ocean was topographically separated from the Panthalassa Ocean by a sill. Comparisons between the flat bottom control and the ridge experiment indicate that the addition of a north-south mid-ocean ridge would likely disrupt of the deep Panthalassa Ocean circulation, causing remarkable changes in vertical mixing. Warm saline water masses from the subtropical region transported into the equatorial zone in the area east of the mid ocean ridge lead to higher water temperatures (by as much as 1.0 degrees C) as well as a decrease in dissolved oxygen concentration. In the experiment with a sill between the Paleo-Tethys and Panthalassa, deep water increased in salinity (by approximately 0.5 psu) and temperature ( approximately 5.0 degrees C). Circulation restriction within the Paleo- Tethys caused by the sill enhanced stratification, leading to a reduced oxygen concentration of these water masses. Both sensitivity experiments indicate that changes in bathymetric features may have been a contributing factor to the Permian-Triassic mass extinction by altering global and regional circulation patterns. 2011-08 Parfenov, L.M., Berzin, N.A., Badarch, G., Dril, S.I., Gerel, O., Goryachev, N.A., Khanchuk, A.I., Kuz'min, M.I., Obolenskiy, A.A., Prokopiev A.V., Ratkin, V.V., Rodionov, S.M., Scotese, C.R., Shpikerman, V.I., TimofeevV.I., Tomurtogoo, O., and Yan Hongquan, 2011. Tectonic and metallogenic model for Northeast Asia, Open File Report. U. S. Geological Survey, OF 2011-1026, Reston, VA. some problem with citation 2011-09 Scotese, C.R., Illich, H., Zumberge, J, and Brown, S., and Moore, T., 2011. The GANDOLPH Project: Year Four Report: Paleogeographic and Paleoclimatic Controls on Hydrocarbon Source Rock Deposition, A report on the Results of the Paleogeographic, Paleoclimatic Simulations (FOAM), and Oils/Source Rock Compilation, Conclusions at the End of Year Four: Oligocene (30 Ma), Cretaceous/Tertiary (70 Ma), Permian/ Triassic (250 Ma), Silurian/Devonian (400 Ma), Cambrian/Ordovician (480 Ma), April, 2011. GeoMark Research Ltd, Houston, Texas, 219 pp. 2011-10 Scotese, C.R. Halifax Arctic 3P 2011-11 Crowley & Scotese, PETM map in National Geographic 2012 2012-01 Chen, Xu, Boucot, A.J., Scotese, C.R., 2012. Pangaean aggregation and disaggregation with evidence from global climate belts, Journal of Paleogeography, vol. 1, pp. 5-13. Abstract: A study of using climate sensitive deposits as a compiled climatic data to locate global climatic belt boundaries through time is developed by the present authors since the 1990s. Global latitudinal belts were presented from Cambrian to Permian as well as the in terval from the early Late Cretaceous to the present. However, during the later Permian and into the Early Cretaceous we noted that the failure of the tropical subtropical belt to penetrate into the interior of Pangaean resulted in the merging of the two arid belts associated with the northern and southern Hadley Cells into one vast, interior arid region. A Pangaeanic paleogeography dominates and obviously affects the climatic distribution from the Late Permian to Early Cretaceous. We employ the dismission and reoccurrence of the global latitudinal climate belts to determine the aggregation and disaggregation of the Pangaean. 2012-02 Scotese, C.R., 2012. The Earth System Archive: a spatial-temporal database describing the evolution of the Earth system since the late Precambrian, 34th International Geological Congress, Abstracts, volume 34, p. 2844. Abstract: The Earth System Archive is a software and GIS package that provides paleoenvironmental information about the Earth's surface during the last 750 million years. The Earth System Archive is built upon the research foundation laid by the GANDOLPH Project and the PALEOMAP PaleoAtlas for ArcGIS. Over 450 paleoenvironmental maps illustrate the evolving Earth System since the late Precambrian. Users of the Earth System Archive will be able to answer questions such as, "How has the elevation of Brisbane changed through time?", or "How has the Mean Surface Temperature of Sydney changed through time?", or "How has the Mean Monthly Rainfall in Papua New Guinea changed through time?". The data used to produce the paleoenvironmental palots will be provided in a digital format compatible with ArcGIS and Excel. The information in the Earth System Archive can serve as fundamental input to basin modeling software, as well as a wide range of geologic, paleontologic, sedimentologic, paleoclimatic and paleooceanographic studies. 2012-03 Main, D.J., Noto, C.R., and C.R. Scotese, 2012. Wildfire paleoecology along the Cretaceous coast of Appalachia, the influence of pale geography and paleoclimate at the Arlington archosaur site, Texas, Geological Society of America, 2012 annual meeting, abstracts with programs, 44:290. Abstract: The Arlington Archosaur Site (AAS) is a fossil locality from the Cretaceous (Cenomanian) Woodbine Formation that occurs in North Texas. The AAS fossil exposures occur within a 2 m section of peat and paleosol. The peat is fossil rich and contains vertebrate fossils of fish, amphibian, turtle, crocodyliform and dinosaur, as well as the remains of numerous trees. Overlying the peat is a paleosol sequence containing dinosaur, crocodyliform, and lungfish. The paleosol contains two distinct horizons. The upper is mottled and well-rooted with numerous calcareous concretions, within which are preserved charcoal, from individual fragments to large stumps and root systems. The lower horizon is a gray mudstone lacking root traces and preserving the majority of the fossils. Concretions likely formed during the dry season, where the water table dropped to the level of the lower horizon, which remained waterlogged year round. The climate in this part of Appalachia during the Cenomanian was generally moist, with a distinct dry season. The beginning of the wet season may have begun with tropical storms that struck the peninsula and sparked wildfires via lightning strikes. The paleogeographic setting was a coastal plain that stretched along a peninsula in the southern interior seaway of southwest Appalachia. We propose the name Rudradia for this paleogeographic peninsula, named for Rudra the storm god. Evidence of wildfires was found via abundant charcoal. Evidence of storms is supported by hummocky beds and a mapped trend seen in the distribution of fossil logs. Charcoal conglomerate beds and numerous fragments are visible throughout the exposed outcrop, occurring below, within, and above the fossil horizons. The presence of charcoal conglomerates is typical of coastal systems where burned materials were transported by river channels. Within the fossil bearing peat bed, > 20 fallen carbonized logs were mapped demonstrating a common NE-SW trend. Above the peat bed, charcoal roots and stumps in the paleosol followed by a charcoal debris flow deposit all lend support to multiple wildfire events that disturbed the coastal ecosystem. We suggest that periodic wildfires were influential in driving diversity at the AAS and provides an opportunity to study the Intermediate Disturbance Hypothesis in a coastal Cretaceous ecosystem. 2012_04 Scotese, C. R., Cryogenian paleogeographic map, p. 393, in Gradstein, Ogg, J.G., Schmitz, M.D., and Ogg, G., 2012. The Geologic Time Scale 2012, volume 1, Elsevier, 435 pp. 2012_05 Scotese, C. R., Cambrian paleogeographic map, p. 437; Ordovician paleogeographic map, p. 489; Silurian paleogeographic map, p. 525; Devonian paleogeographic map, p. 559; Carboniferous paleogeographic map, p. 603; Permian paleogeographic map, p. 653; Triassic paleogeographic map, p. 681; Jurassic paleogeographic map, p. 731; Cretaceous paleogeographic map, p. 793; Paleogene paleogeographic map, p. 855; Neogene paleogeographic map, p. 923; Quaternary paleogeographic map, p. 979; in Gradstein, Ogg, J.G., Schmitz, M.D., and Ogg, G., 2012. The Geologic Time Scale 2012, volume 2, Elsevier, 1144 pp. 2012-06 Scotese, C.R., Wegener Symposium Inroduction 2012-07 Scotese, C.R. Continental Drift: The Idea that Changed the World 2012-08 Scotese, C.R. Paleogeographic . . . . Circum Arctic 2012-09 CRS DGS Talk 2013 2013-01 Chatterjee, S., Goswami, A., and C.R. Scotese, 2013. The longest voyage: Tectonic, magmatic, and paleoclimatic evolution of the Indian plate during its northward flight from Gondwana to Asia, Gondwana Research, 23: 238-267. (116) Abstract: The tectonic evolution of the Indian Plate, which started in Late Jurassic about 167 million years ago (approximately 167Ma) with the breakup of Gondwana, presents an exceptional and intricate case history against which a variety of plate tectonic events such as: continental breakup, sea-floor spreading, birth of new oceans, flood basalt volcanism, hotspot tracks, transform faults, subduction, obduction, continental collision, accretion, and mountain building can be investigated. Plate tectonic maps are presented here illustrating the repeated rifting of the Indian plate from surrounding Gondwana continents, its northward migration, and its collision first with the Kohistan-Ladakh Arc at the Indus Suture Zone, and then with Tibet at the Shyok - Tsangpo Suture. The associations between flood basalts and the recurrent separation of the Indian plate from Gondwana are assessed. The breakup of India from Gondwana and the opening of the Indian Ocean is thought to have been caused by plate tectonic forces which were localized along zones of weakness caused by mantle plumes (Bouvet, Marion, Kerguelen, and Reunion Plumes). The sequential spreading of the Southwest Indian Ridge/Davie Ridge, Southeast Indian Ridge, Central Indian Ridge, Palitana Ridge, and Carlsberg Ridge in the Indian Ocean were responsible for the fragmentation of the Indian Plate during the Late Jurassic and Cretaceous times. The Reunion and the Kerguelen Plumes left two spectacular hotspot tracks on either side of the Indian Plate. With the breakup of Gondwana, India remained isolated as an island continent, but reestablished its biotic links with Africa during the Late Cretaceous during its collision with the Kohistan-Ladakh Arc ( approximately 85Ma) along the Indus Suture. Soon after the Deccan eruption, India drifted northward as an island continent by rapid motion carrying Gondwana biota, about 20cm/year, between 67Ma to 50Ma; it slowed down dramatically to 5cm/year during its collision with Asia in early Eocene ( approximately 50Ma). A northern corridor was established between India and Asia soon after the collision allowing faunal interchange. This is reflected by mixed Gondwana and Eurasian elements in the fossil record preserved in several continental Eocene formations of India. A revised India-Asia collision model suggests that the Indus Suture represents the obduction zone between India and the Kohistan-Ladakh Arc, whereas the Shyok Suture represents the collision between the Kohistan-Ladakh Arc and Tibet. Eventually, the Indus-Tsangpo Zone became the locus of the final India-Asia collision, which probably began in early Eocene ( approximately 50Ma) with the closure of Neotethys Ocean. The post-collisional tectonics for the last 50 million years is best expressed in the evolution of the Himalaya-Tibetan Orogen. The great thickness of crust beneath Tibet and Himalaya and a series of north vergent thrust zones in the Himalaya and the south-vergent subduction zones in Tibetan Plateau suggest the progressive convergence between India and Asia of about 2500km since the time of collision. In the early Eohimalayan phase ( approximately 50 to 25Ma) of Himalayan Orogeny (middle Eocene-late Oligocene), thick sediments on the leading edge of the Indian Plate were squeezed, folded, and faulted to form the Tethyan Himalaya. With continuing convergence of India, the architecture of the Himalayan - Tibetan Orogen is dominated by deformational structures developed in the Neogene Period during the Neohimalayan phase ( approximately 21Ma to present), creating a series of north-vergent thrust belt systems such as the Main Central Thrust, the Main Boundary Thrust, and the Main Frontal Thrust to accommodate crustal shortening. Neogene molassic sediment shed from the rise of the Himalaya was deposited in a nearly continuous foreland trough in the Siwalik Group containing rich vertebrate assemblages. Tomographic imaging of the India-Asia Orogen reveals that Indian lithospheric slab has been subducted subhorizontally beneath the entire Tibetan Plateau that has played a key role in the uplift of the Tibetan Plateau. The low-viscosity channel flow in response to topographic loading of Tibet provides a mechanism to explain the Himalayan-Tibetan Orogen. From the start of its voyage in Southern Hemisphere, to its final impact with the Asia, the Indian Plate has experienced changes in climatic conditions both short-term and long-term. We present a series of paleoclimatic maps illustrating the temperature and precipitation conditions based on estimates of Fast Ocean Atmospheric Model, a coupled global climate model. The uplift of the Himalaya- Tibetan Plateau above the snow line created two most important global climate phenomena-the birth of the Asian monsoon and the onset of Pleistocene glaciation. As the mountains rose, and the monsoon rains intensified, increasing erosional sediments from the Himalaya were carried down by the Ganga River in the east and the Indus River in the west, and were deposited in two great deep-sea fans, the Bengal and the Indus. Vertebrate fossils provide additional resolution for the timing of three crucial tectonic events: India-KL Arc collision during the Late Cretaceous, India-Asia collision during the early Eocene, and the rise of the Himalaya during the early Miocene. 2013-02 Osen, A., Winguth, A., Winguth, C., and C.R. Scotese, 2013. Sensitivity of Late Permian climate to bathymetric features and implications for the mass extinction, Global and Planetary Change, 105:171-179. (117) Abstract: Evidence from stratigraphic sections of the Panthalassa, Paleo-Tethys and Neo-Tethys suggests that the oceans experienced widespread anoxia during the Late Permian, which likely contributed to the extinction of approximately 90% of marine and approximately 70% of terrestrial species. The Late Permian and Early Triassic were also characterized by significant carbon isotope excursions implying that considerable perturbations in the carbon cycle occurred. Bathymetric features of the Panthalassa during this period are not well known since most of the ocean floor has been subducted; however, tectonic reconstructions suggest that active marine subduction zones surrounded Pangea. Thus, it is reasonable to assume that there was an active mid-ocean ridge system located in Panthalassa during the Late Permian. In this study, the impact of such a spreading center within Panthalassa on the climate and carbon cycle is investigated using a comprehensive climate system model for the end-Permian. This is a novel approach because a majority of previous simulations assumed a flat bottom for the Panthalassa deep-sea. The mid-ocean ridge (MOR) simulation enhanced vertical mixing and topographic steering of the currents near the ridge-axis but in comparison with the simulation using a flat bottom, changes in the global distribution of water masses and circulation in the Panthalassa were insignificant. Dissolved oxygen concentrations were not considerably affected by the implementation of the midocean ridge. Thus the approximation of using a flat-bottom topography in ocean models for the Late Permian remains valid. In a second sensitivity study, the effect of a sill between the deep Paleo-Tethys and Panthalassa on water mass distribution and oxygen content has been investigated. Model results suggest that the introduction of a sill led to enhanced stratification, as well as an increase in salinity and temperature in the Paleo- Tethys. An associated reduction of the dissolved oxygen concentration to dysoxic to near-anoxic conditions below 1800m suggests that the changes in sill height between the Paleo-Tethys and Panthalassa may have been a contributing factor of regional importance to the Permian-Triassic mass extinction 2013-03 Boucot, A.J., Chen Xu, and Scotese, C.R, 2013. Phanerozoic Paleoclimate: An Atlas of Lithologic Indicators of Climate, SEPM Concepts in Sedimentology and Paleontology, (Print-on-Demand Version), No. 11, 478 pp., ISBN 978-1-56576-289-3, October 2013, Society for Sedimentary Geology, Tulsa, OK. This publication combines the interpretations of two major sets of data. One is the geophysical data that is used to interpret the position of the tectonic plates through geologic time. The other is based on a long time search of the geological literature to find, record and evaluate the lithologic descriptions of countless reports around the globe; paying careful attention to those lithologies that have climatic implications. The introduction to this volume includes a detailed discussion of the lithologies, mineralogies and biogeographies that are considered to be the most reliable in identifying the climatic conditions existing during their formation and how they are used or not used in this compilation. These include coal, cyclothems, laterite, bauxite, lateritic manganese, oolitic ironstone, kaolin, glendonite, tillites, dropstones, calcretes, evaporites, clay minerals, palms, mangroves, and crocodilians. Additionally, several others are discussed but not used for specified reasons. These include eolian sandstone, silcrete and some specific paleobotanical methodologies. Global paleoclimatic zones based on the climatically interpreted data points are identified during twenty-eight time periods from Cambrian to Miocene using paleotectonic reconstructed maps. The paleoclimate of each time period is summarized and includes a discussion of the specific referenced data points that have been interpreted to be the most reliable available for that time period and location. 2013-04 Boucot, A.J., Chen Xu, and Scotese, C.R, 2013. Phanerozoic Paleoclimate: An Atlas of Lithologic Indicators of Climate, SEPM Concepts in Sedimentology and Paleontology, (Digital Version), No. 11, 478 pp., ISBN 978-1-56576-281-7, October 2013 Society for Sedimentary Geology, Tulsa, OK. This publication combines the interpretations of two major sets of data. One is the geophysical data that is used to interpret the position of the tectonic plates through geologic time. The other is based on a long time search of the geological literature to find, record and evaluate the lithologic descriptions of countless reports around the globe; paying careful attention to those lithologies that have climatic implications. The introduction to this volume includes a detailed discussion of the lithologies, mineralogies and biogeographies that are considered to be the most reliable in identifying the climatic conditions existing during their formation and how they are used or not used in this compilation. These include coal, cyclothems, laterite, bauxite, lateritic manganese, oolitic ironstone, kaolin, glendonite, tillites, dropstones, calcretes, evaporites, clay minerals, palms, mangroves, and crocodilians. Additionally, several others are discussed but not used for specified reasons. These include eolian sandstone, silicrete and some specific paleobotanical methodologies. Global paleoclimatic zones based on the climatically interpreted data points are identified during twenty-eight time periods from Cambrian to Miocene using paleotectonic reconstructed maps. The paleoclimate of each time period is summarized and includes a discussion of the specific referenced data points that have been interpreted to be the most reliable available for that time period and location. 2013-05 Boucot, A.J., Chen Xu, and Scotese, C.R, 2013. Phanerozoic Paleoclimate: An Atlas of Lithologic Indicators of Climate, SEPM Concepts in Sedimentology and Paleontology, (Printed Map Folio), No. 11, 478 pp., ISBN 978-1-56576-282-4, October 2013, Society for Sedimentary Geology, Tulsa, OK. This publication combines the interpretations of two major sets of data. One is the geophysical data that is used to interpret the position of the tectonic plates through geologic time. The other is based on a long time search of the geological literature to find, record and evaluate the lithologic descriptions of countless reports around the globe; paying careful attention to those lithologies that have climatic implications. The introduction to this volume includes a detailed discussion of the lithologies, mineralogies and biogeographies that are considered to be the most reliable in identifying the climatic conditions existing during their formation and how they are used or not used in this compilation. These include coal, cyclothems, laterite, bauxite, lateritic manganese, oolitic ironstone, kaolin, glendonite, tillites, dropstones, calcretes, evaporites, clay minerals, palms, mangroves, and crocodilians. Additionally, several others are discussed but not used for specified reasons. These include eolian sandstone, silcrete and some specific paleobotanical methodologies. Global paleoclimatic zones based on the climatically interpreted data points are identified during twenty-eight time periods from Cambrian to Miocene using paleotectonic reconstructed maps. The paleoclimate of each time period is summarized and includes a discussion of the specific referenced data points that have been interpreted to be the most reliable available for that time period and location. 2013-06 Scotese, C.R., Moore, T.L., and C.T. Dreher, 2013. Teaching and research tools for deep time studies: Ancient Earth app, Global Geology website, and the PALEOMAP PaleoAtlas for ArcGIS, Geological Society of America annual meeting, abstracts with programs, v. 45, p. 233. (115) Abstract: Three new software tools are now available for deep time research studies and teaching: the Ancient Earth app, www.globalgeology.com, and the PALEOMAP PaleoAtlas for Arc GIS. The simplest and easiest tool to use is the Ancient Earth app developed for the iPad/iPhone. Ancient Earth allows users to view the changing plate tectonic, paleogeographic and paleoclimatic history of the Earth on a series of paleoglobes that can be rescaled and rotated interactively. A special "bookmark" tool allows users to build tutorials that focus on the geological history of specific regions or geologic features (e.g. Reunion hotspot, Appalachian mountains). The website globalgeology.com, has two major functions. It is a global database consisting of >500,000 stratigraphic records that describe the lithologic and paleoenvironmental history of the Earth. Visitors to the website can browse the global geology database or enter new stratigraphic information. The website also allows users to plot this geological information on downloadable, Google Earth-style, "paleoglobes". Paleoglobes are reconstructions of the ancient earth that show the past positions of the continents, along with the changing distribution of mountains, shallow seas, and other features through time. The Global Geology Paleoglobe tool lets you select a time interval and download a Google Earth- style paleoglobe (kmz format) that illustrates a variety of features, such as: paleotopography , paleobathymetry, plate tectonic boundaries, paleowinds, paleotemperature, or ancient oceanic circulation. You can add stratigraphic information from the Global Geology database or plot user-defined localities that appear as pins on a interactive Google Earth display. The third research/teaching tool is the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas consists of 50 paleoreconstructions (shapefiles) illustrating the plate tectonic history of the Earth since the Late Precambrian. Using the program, PointTracker, users can plot reconstructed, user-defined locality data on the paleoreconstructions. 2013-07 Scotese, C.R., 2013. Map Folio 1, Present-day (Holocene, 0 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-08 Scotese, C.R., 2013. Map Folio 2, Last Glacial Maximum (Pleistocene, 21 ky), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-09 Scotese, C.R., 2013. Map Folio 3, Pliocene (Zanclean&Piacenzian, 3.7 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-10 Scotese, C.R., 2013. Map Folio 4, latest Miocene (Messinian, 6.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-11 Scotese, C.R., 2013. Map Folio 5, Middle/Late Miocene (Serravallian & Tortonian, 10.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-12 Scotese, C.R., 2013. Map Folio 6, Middle Miocene (Langhian, 14.9 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-13 Scotese, C.R., 2013. Map Folio 7, Early Miocene (Aquitanian & Burdigalian, 19.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-14 Scotese, C.R., 2013. Map Folio 8, Late Oligocene (Chattian, 25.7 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-15 Scotese, C.R., 2013. Map Folio 9, Early Oligocene (Rupelian, 31.1 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-16 Scotese, C.R., 2013. Map Folio 10, Late Eocene (Priabonian, 35.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-17 Scotese, C.R., 2013. Map Folio 11, late Middle Eocene (Bartonian, 38.8 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-18 Scotese, C.R., 2013. Map Folio 12, early Middle Eocene (middle Lutetian, 44.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-19 Scotese, C.R., 2013. Map Folio 13, Early Eocene (Ypresian, 52.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-20 Scotese, C.R., 2013. Map Folio 14, Paleocene/Eocene Boundary (Thanetian/Ypresian Boundary, 55.8 Ma) PETM, PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-21 Scotese, C.R., 2013. Map Folio 15, Paleocene (Danian & Thanetian, 60.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 1, Cenozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-22 Scotese, C.R., 2013. Map Folio 16, KT Boundary (latest Maastrichtian, 65.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-23 Scotese, C.R., 2013. Map Folio 17, Late Cretaceous (Maastrichtian, 68 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-24 Scotese, C.R., 2013. Map Folio 18, Late Cretaceous (Late Campanian, 73.8 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-25 Scotese, C.R., 2013. Map Folio 19, Late Cretaceous (Early Campanian, 80.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-26 Scotese, C.R., 2013. Map Folio 20, Late Cretaceous (Santonian & Coniacian, 86 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-27 Scotese, C.R., 2013. Map Folio 21, Mid-Cretaceous (Turonian , 91.1 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-28 Scotese, C.R., 2013. Map Folio 22, Mid-Cretaceous (Cenomanian, 96.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-29 Scotese, C.R., 2013. Map Folio 23, Early Cretaceous (late Albian, 101.8 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-30 Scotese, C.R., 2013. Map Folio 24, Early Cretaceous (middle Albian, 106 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-31 Scotese, C.R., 2013. Map Folio 25, Early Cretaceous (early Albian, 110 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-32 Scotese, C.R., 2013. Map Folio 26, Early Cretaceous (late Aptian, 115.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-33 Scotese, C.R., 2013. Map Folio 27, Early Cretaceous (early Aptian, 121.8 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-34 Scotese, C.R., 2013. Map Folio 28, Early Cretaceous (Barremian, 127.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-35 Scotese, C.R., 2013. Map Folio 29, Early Cretaceous (Hauterivian, 132 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-36 Scotese, C.R., 2013. Map Folio 30, Early Cretaceous (Valanginian, 137 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-37 Scotese, C.R., 2013. Map Folio 31, Early Cretaceous (Berriasian, 143 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-38 Scotese, C.R., 2013. Map Folio 32, Jurassic/Cretaceous Boundary (145.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 2, Cretaceous Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-39 Scotese, C.R., 2013. Map Folio 33, Late Jurassic (Tithonian, 148.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-40 Scotese, C.R., 2013. Map Folio 34, Late Jurassic (Kimmeridgian, 153.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-41 Scotese, C.R., 2013. Map Folio 35, Late Jurassic (Oxfordian, 158.4 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-42 Scotese, C.R., 2013. Map Folio 36, Middle Jurassic (Callovian, 164.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-43 Scotese, C.R., 2013. Map Folio 37, Middle Jurassic (Bajocian&Bathonian, 169.7), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-44 Scotese, C.R., 2013. Map Folio 38, Middle Jurassic (Aalenian, 173.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-45 Scotese, C.R., 2013. Map Folio 39, Early Jurassic (Toarcian, 179.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-46 Scotese, C.R., 2013. Map Folio 40, Early Jurassic (Pliensbachian, 186.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-47 Scotese, C.R., 2013. Map Folio 41, Early Jurassic (Sinemurian, 193 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-48 Scotese, C.R., 2013. Map Folio 42, Early Jurassic (Hettangian, 198 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-49 Scotese, C.R., 2013. Map Folio 43, Triassic-Jurassic Boundary (199.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-50 Scotese, C.R., 2013. Map Folio 44, Late Triassic (Norian, 210 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-51 Scotese, C.R., 2013. Map Folio 45, Late Triassic (Carnian, 222.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-52 Scotese, C.R., 2013. Map Folio 46, Middle Triassic (Ladinian, 232.9 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-53 Scotese, C.R., 2013. Map Folio 47, Middle Triassic (Anisian, 241.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-54 Scotese, C.R., 2013. Map Folio 48, Early Triassic (Induan & Olenekian, 248.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 3, Triassic and Jurassic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-55 Scotese, C.R., 2013. Map Folio 49, Permo-Triassic Boundary (251 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-56 Scotese, C.R., 2013. Map Folio 50, Late Permian (Lopingian, 255.7 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-57 Scotese, C.R., 2013. Map Folio 51, late Middle Permian (Capitanian, 263.1 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-58 Scotese, C.R., 2013. Map Folio 52, Middle Permian (Roadian & Wordian, 268.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-59 Scotese, C.R., 2013. Map Folio 53, Early Permian (Kungurian, 273.1 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-60 Scotese, C.R., 2013. Map Folio 54, Early Permian (Artinskian, 280 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-61 Scotese, C.R., 2013. Map Folio 55, Early Permian (Sakmarian, 289.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-62 Scotese, C.R., 2013. Map Folio 56, Early Permian (Asselian, 296.8 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-63 Scotese, C.R., 2013. Map Folio 57, Late Pennsylvanian (Gzhelian, 301.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-64 Scotese, C.R., 2013. Map Folio 58, Late Pennsylvanian (Kasimovian, 305.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-65 Scotese, C.R., 2013. Map Folio 59, Middle Pennsylvanian (Moscovian, 309.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-66 Scotese, C.R., 2013. Map Folio 60, Early Pennsylvanian (Bashkirian, 314.9 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-67 Scotese, C.R., 2013. Map Folio 61, Late Mississippian (Serpukhovian, 323.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-68 Scotese, C.R., 2013. Map Folio 62, Middle Mississippian (late Visean, 332.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-69 Scotese, C.R., 2013. Map Folio 63, Middle Mississippian (early Visean, 341.1 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-70 Scotese, C.R., 2013. Map Folio 64, Early Mississippian (Tournaisian, 352.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-71 Scotese, C.R., 2013. Map Folio 65, Devono-Carboniferous Boundary (359.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-72 Scotese, C.R., 2013. Map Folio 66, Late Devonian (early Famennian, 370.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-73 Scotese, C.R., 2013. Map Folio 67, Late Devonian (Frasnian, 379.9 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-74 Scotese, C.R., 2013. Map Folio 68, Middle Devonian (Givetian, 388.2 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-75 Scotese, C.R., 2013. Map Folio 69, Middle Devonian (Eifelian, 394.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-76 Scotese, C.R., 2013. Map Folio 70, Early Devonian (Emsian, 402.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-77 Scotese, C.R., 2013. Map Folio 71, Early Devonian (Pragian, 409.1 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-78 Scotese, C.R., 2013. Map Folio 72, Early Devonian (Lochkovian, 413.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 4, Late Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-79 Scotese, C.R., 2013. Map Folio 73, Late Silurian (Ludlow & Pridoli, 419.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-80 Scotese, C.R., 2013. Map Folio 74, Middle Silurian (Wenlock, 425.6 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-81 Scotese, C.R., 2013. Map Folio 75, Early Silurian (late Llandovery, 432.1 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-82 Scotese, C.R., 2013. Map Folio 76, Early Silurian (early Llandovery, 439.8 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-83 Scotese, C.R., 2013. Map Folio 77, Late Ordovician (Hirnantian, 444.7 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-84 Scotese, C.R., 2013. Map Folio 78, Late Ordovician (Ashgill, 448.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-85 Scotese, C.R., 2013. Map Folio 79, Late Ordovician (Caradoc, 456 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-86 Scotese, C.R., 2013. Map Folio 80, Middle Ordovician (Darwillian,464.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-87 Scotese, C.R., 2013. Map Folio 81, Early Ordovician (Arenig, 473.4 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-88 Scotese, C.R., 2013. Map Folio 82, Early Ordovician (Tremadoc, 480 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-89 Scotese, C.R., 2013. Map Folio 83, XXX, PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-90 Scotese, C.R., 2013. Map Folio 84, Cambro-Ordovician Boundary (488.3 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-91 Scotese, C.R., 2013. Map Folio 85, Late Cambrian (Furongian, 494 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-92 Scotese, C.R., 2013. Map Folio 86, Middle Cambrian (510 520 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-93 Scotese, C.R., 2013. Map Folio 87, Early Cambrian (531.5 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-94 Scotese, C.R., 2013. Map Folio 88, Cambrian/Precambrian boundary (542 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-95 Scotese, C.R., 2013. Map Folio 89, Late Neoproterozoic (late Ediacaran, 560 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-96 Scotese, C.R., 2013. Map Folio 90, Late Neoproterozoic (Middle Ediacaran, 600 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-97 Scotese, C.R., 2013. Map Folio 91, Late Neoproterozoic (Early Ediacaran, 650 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-98 Scotese, C.R., 2013. Map Folio 92, Middle Neoproterozoic (Late Cryogenian, 690 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-99 Scotese, C.R., 2013. Map Folio 93, Middle Neoproterozoic (Middle Cryogenian, 750 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-100 Scotese, C.R., 2013. Map Folio 94, Early Neoproterozoic (Tonian, 900 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-101 Scotese, C.R., 2013. Map Folio 95, Late Mesoproterozoic (Stenian, 1100 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-102 Scotese, C.R., 2013. Map Folio 96, Middle Mesoproterozoic (Ectasian, 1300 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-103 Scotese, C.R., 2013. Map Folio 97, Early Mesoproterozoic (Calymmian, 1500 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-104 Scotese, C.R., 2013. Map Folio 98, Late Paleoproterozoic (Statherian, 1700 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-105 Scotese, C.R., 2013. Map Folio 99, Middle Paleoproterozoic (Orosirian, 1900 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-106 Scotese, C.R., 2013. Map Folio 100, Middle Paleoproterozoic (Rhyacian, 2100 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-107 Scotese, C.R., 2013. Map Folio 101, Early Paleoproterozoic (Siderian, 2400 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-108 Scotese, C.R., 2013. Map Folio 102, Archean (4000 - 2500 Ma) PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2013-109 Scotese, C.R., 2013. Map Folio 103, Hadean (4600 - 4000 Ma) PALEOMAP PaleoAtlas for ArcGIS, volume 6, Precambrian, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL. 2014 ArcGIS Atlases 2014-01 Scotese, C.R., 2014, The PALEOMAP Project PaleoAtlas for ArcGIS, version 2, Volume 1, Cenozoic Plate Tectonic, Paleogeographic, and Paleoclimatic Reconstructions, Maps 1-15, PALEOMAP Project, Arlington, Texas. 2014-02 Scotese, C.R., 2014, The PALEOMAP Project PaleoAtlas for ArcGIS, version 2, Volume 2, Cretaceous Plate Tectonic, Paleogeographic, and Paleoclimatic Reconstructions, Maps 16-32, PALEOMAP Project, Arlington, Texas. 2014-03 Scotese, C.R., 2014, The PALEOMAP Project PaleoAtlas for ArcGIS, version 2, Volume 3, Triassic and Jurassic Plate Tectonic, Paleogeographic, and Paleoclimatic Reconstructions, Maps 33-48, PALEOMAP Project, Arlington, Texas. 2014-04 Scotese, C.R., 2014, The PALEOMAP Project PaleoAtlas for ArcGIS, version 2, Volume 4, Late Paleozoic Plate Tectonic, Paleogeographic, and Paleoclimatic Reconstructions, Maps 49-74, PALEOMAP Project, Arlington, Texas. 2014-05 Scotese, C.R., 2014, The PALEOMAP Project PaleoAtlas for ArcGIS, version 2, Volume 5, Early Paleozoic Plate Tectonic, Paleogeographic, and Paleoclimatic Reconstructions, Maps 75-88, PALEOMAP Project, Arlington, Texas. 2014-06 Scotese, C.R., 2014, The PALEOMAP Project PaleoAtlas for ArcGIS, version 2, Volume 6, Precambrian Plate Tectonic, Paleogeographic, and Paleoclimatic Reconstructions, Maps 89- 103. PALEOMAP Project, Arlington, Texas. Paleogeographic Mini-Atlases (Mollweide) 2014-07 Scotese, C.R., 2014. Atlas of Neogene Paleogeographic Maps (Mollweide Projection), Maps 1-7, Volume 1, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-08 Scotese, C.R., 2014. Atlas of Paleogene Paleogeographic Maps (Mollweide Projection), Maps 8-15, Volume 1, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-09 Scotese, C.R., 2014. Atlas of Late Cretaceous Paleogeographic Maps, PALEOMAP Atlas for ArcGIS, volume 2, The Cretaceous, Maps 16 ╨ 22, Mollweide Projection, PALEOMAP Project, Evanston, IL. 2014-10 Scotese, C.R., 2014. Atlas of Early Cretaceous Paleogeographic Maps, PALEOMAP Atlas for ArcGIS, volume 2, The Cretaceous, Maps 23-31, Mollweide Projection, PALEOMAP Project, Evanston, IL. 2014-11 Scotese, C.R., 2014. Atlas of Jurassic Paleogeographic Maps, PALEOMAP Atlas for ArcGIS, volume 3, The Jurassic and Triassic, Maps 32-42, Mollweide Projection, PALEOMAP Project, Evanston, IL. 2014-12 Scotese, C.R., 2014. Atlas of Middle & Late Permian and Triassic Paleogeographic Maps, maps 43 - 48 from Volume 3 of the PALEOMAP Atlas for ArcGIS (Jurassic and Triassic) and maps 49 – 52 from Volume 4 of the PALEOMAP PaleoAtlas for ArcGIS (Late Paleozoic), Mollweide Projection, PALEOMAP Project, Evanston, IL. 2014-15 Scotese, C.R., 2014. Atlas of Permo-Carboniferous Paleogeographic Maps (Mollweide Projection), Maps 53 – 64, Volume 4, The Late Paleozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-16 Scotese, C.R., 2014. Atlas of Devonian Paleogeographic Maps, PALEOMAP Atlas for ArcGIS, volume 4, The Late Paleozoic, Maps 65-72, Mollweide Projection, PALEOMAP Project, Evanston, IL. 2014-17 Scotese, C.R., 2014. Atlas of Silurian and Middle-Late Ordovician Paleogeographic Maps (Mollweide Projection), Maps 73 – 80, Volumes 5, The Early Paleozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-18 Scotese, C.R., 2014. Atlas of Cambrian and Early Ordovician Paleogeographic Maps (Mollweide Projection), Maps 81-88, Volumes 5, The Early Paleozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Topical Atlases (Rectilinear) 2014-19 Scotese, C.R., Boucot, A.J, and Chen Xu, 2014. Atlas of Phanerozoic Climatic Zones (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-20 Scotese, C.R., and Moore, T.L., 2014. Atlas of Phanerozoic Temperatures (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-21 Scotese, C.R. and Moore, T.L., 2014. Atlas of Phanerozoic Rainfall (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-22 Scotese, C.R., and Moore, T.L., 2014. Atlas of Phanerozoic Ocean Currents and Salinity (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-23 Scotese, C.R., and Moore, T.L., 2014. Atlas of Phanerozoic Oceanic Anoxia (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-24 Scotese, C.R., and Moore, T.L., 2014. Atlas of Phanerozoic Upwelling Zones (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-25 Scotese, C.R., 2014. Atlas of Plate Tectonic Reconstructions (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. 2014-26 Rose et al. in Nature 2015 Precambrian Atlas Scotese, C.R., 2015. Atlas of Precambrian Paleogeographic Maps (Mollweide Projection), Maps 89-103, Volumes 6, The Precambrian, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Future Atlas Scotese, C.R., 2015. Atlas of Future Paleogeographic Maps (Mollweide Projection), Volumes 7, The Future, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Simplified Paleogeographic Maps (Rectilinear) Scotese, C.R., 2015. Atlas of Cenozoic (Simplified) Paleogeographic Maps (Mollweide Projection), Maps 1-15, Volume 1, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Scotese, C.R., 2015. Atlas of Mesozoic (Simplified) Paleogeographic Maps (Mollweide Projection), Maps 16–48, Volumes 2&3, The Cretaceous & Jurassic and Triassic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Scotese, C.R., 2015. Atlas of Paleozoic (Simplified) Paleogeographic Maps (Mollweide Projection), Maps 49-88, Volume 4&5, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Scotese, C.R., 2015. Atlas of Precambrian (Simplified) Paleogeographic Maps (Mollweide Projection), Maps 89-103, Volume 6, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Basemaps (Rectilinear) Scotese, C.R., 2015. Atlas of Phanerozoic Basemaps (Mollweide Projection), Maps 1-7, Volume 1, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Geological Maps (Rectilinear) Scotese, C.R., 2015. Atlas of Cenozoic Geological Maps (Mollweide Projection), Maps 1-15, Volume 1, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Scotese, C.R., 2015. Atlas of Mesozoic 3 Geological Maps (Mollweide Projection), Maps 16-48, Volume 2&3, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Scotese, C.R., 2015. Atlas of Paleozoic Geological Maps (Mollweide Projection), Maps 49-88, Volume 4&5, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project Evanston, IL. Scotese, C.R., 2015. Atlas of Precambrian Geological Maps (Mollweide Projection), Maps 89-103, Volume 6, The Cenozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL. Climatic Reconstructions Scotese, C.R., 2015. Atlas of Phanerozoic Climatic Reconstructions (Mollweide Projection), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL. Winds Scotese, C.R., 2015. Atlas of Phanerozoic Winds (Rectilinear Projectioon), Volumes 1-6, PALEOMAP Project PaleoAtlas for ArcGIS, PALEOMAP Project, Evanston, IL.