Paleogeography

This map folio should be referenced as:
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.

Introduction
These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

Yıllardır ülkemizin doğal-tarihsel-kültürel kimliğine belirli boyutlarda bakmanın gerekliliği üzerinde sürekli durmaya, belirli örneklerle bunun "kaçınılmaz olduğunu" kanıtlamaya çalışıyoruz. Bu konuda başarılı olduğumuz havzaların kazandırdığı deneyimlerden kalkarak, son yıllarda ülke bütününe yönelme şansımız oldu.

Küçük Menderes AraĢtırmaları (KÜMAR) Kerschner M. (1995) Ostgriechische Vogelschalen und Verwandtes. Studien zur Chronologie und Verbreitung der ostgriechischen Keramik (ungedr. Diss. Universitat Bochum). Kerschner M. (1997) Ein stratifizierter Opferkomplex des 7. Jh.s v. Chr. aus dem Artemision von Ephesos, OJh 66, Beibl. 85-226.

Copyright 2009, Society of Petroleum Engineers This paper was prepared for presentation at the 2009 SPE/EAGE Reservoir Characterization and Simulation Conference held in Abu Dhabi, UAE, 19–21 October 2009. This paper was selected for presentation by an SPE ...

Accurately mapping plate boundary types and locations through time is essential for understanding the evolution of the plate-mantle system and the exchange of material between the solid Earth and surface environments. However, the complexity of the Earth system and the cryptic nature of the geological record make it difficult to discriminate tectonic environments through deep time. Here we present a new method for identifying tectonic paleo-environments on Earth through a data mining approach using global geochemical data. We first fingerprint a variety of present-day tectonic environments utilising up to 136 geochemical data attributes in any available combination. A total of 38301 geochemical analyses from basalts aged from 5e0 Ma together with a well-established plate reconstruction model are used to construct a suite of discriminatory models for the first order tectonic environments of subduction and mid-ocean ridge as distinct from intraplate hotspot oceanic environments, identifying 41, 35, and 39 key discriminatory geochemical attributes, respectively. After training and validation, our model is applied to a global geochemical database of 1547 basalt samples of unknown tectonic origin aged between 1000 e410 Ma, a relatively ill-constrained period of Earth's evolution following the breakup of the Rodinia supercontinent, producing 56 unique global tectonic environment predictions throughout the Neo-proterozoic and Early Paleozoic. Predictions are used to discriminate between three alternative published Rodinia configuration models, identifying the model demonstrating the closest spatio-temporal consistency with the basalt record, and emphasizing the importance of integrating geochemical data into plate reconstructions. Our approach offers an extensible framework for constructing full-plate, deep-time reconstructions capable of assimilating a broad range of geochemical and geological observations, enabling next generation Earth system models.

The Cuchilla Dionisio Terrane (CDT) is part of the Arachania paleocontinent and is divided into two sections separated by the Laguna Merin Basin. The northern sector is the least known and for which less geochronological information is available. The oldest dated unit in the sector are the Mendizábal Ortogneisses, for which a concordant U-Pb SIMS age on zircon of 664 ± 2 Ma was obtained. This age coincides with a U-Pb SHRIMP age of 674 ± 7 Ma for deformed ortogneisses in the Sarandi de Barceló area. Granites with ages around 630 Ma crop out extensively in the N and W. The Sarandí de Yaguarón Granite and the Arroyo Malo Granite yielded zircon ages of 630 ± 8 Ma (U-Pb SHRIMP) and 625 ± 10 Ma (U-Pb SIMS), respectively. A muscovite granite deformed by the Cerros de Amaro Lineament, dated U-Pb SIMS on zircon at 628 ± 3 Ma, may represent a deformed border of the Arroyo Malo Granite. At 600 Ma ago the opening of a basin with oceanic crust generation is recorded, whose fragments are represented by mafic and ultramafic rocks of the Cerro de la Tuna, included here in the Paso del Dragón Formation. These are juvenile rocks with N-MORB affinity, TDM between 660 and 570 Ma and Nd between +8.2 and +9.4. Siliciclastic rocks of the Paso del Dragón Formation were deposited in this basin and yielded detrital zircon U-Pb SIMS ages showing Eburnean (1954-1804 Ma, 36%), Namaqualand (10%) and Neoproterozoic (738-626 Ma, 23%) sources. This basin may correspond to the  Marmora back-arc basin, in which the Rocha Formation and its equivalents in southern Africa were also deposited. The depositional age is best constrained at 588 Ma by reported ages of synsedimentary volcanism. Later, the intrusion of several granitoids took place, namely: Tacuarí (585 ± 3 Ma), Asperezas (580 ± 10 Ma) and the Cuchilla Dionsio Batholith, for which a concordant U-Pb SIMS zircon age of 577 ± 2 Ma is reported. This magmatism affects the entire northern part of the CDT and partly overlaps in age with the Aiguá Batholith. Acid volcanism of Sierra de Ríos Formation in the north (575 ± 14 Ma, Rb-Sr) and the Cerros de Aguirre Formation in the southern CDT is clearly associated with this phase of magmatism. By 530 Ma tangential collision of the CDT with the Río de la Plata Craton occurred through the Sierra Ballena Shear Zone. Thrusts with NNW vergence were also generated, such as the Sarandí de Barceló and Amarillo thrusts. The data here presented confirm the view of the CDT as an allochthonous terrane rifted off the Kalahari Craton at 750 Ma, which later evolved into a magmatic arc. The CDT was unrelated to the Río de la Plata Craton until its tangential collision with it at ca. 530 Ma.

The paleotectonic and volcanic features of the Jurassic-Cretaceous carbonate successions, outcropping in central-western Sicily, allow us to restore the tectono-sedimentary evolution of a sector of the African continental margin. These successions consist of shallow-to-deep-water Mesozoic deposits that have formed in the carbonate platform-to-pelagic plateau depositional setting of the so-called Trapanese paleogeographic domain. Fieldwork, including structural analyses, has indicated the occurrence of lateral facies changes, resedimented materials, volcanic products (pillow lavas and tuffitic deposits), unconformity surfaces and paleofaults of different trends and age. These data, combined with facies and a physical-stratigraphic analysis, allow one to distinguish between the different tectono-stratigraphic settings. A structural low, filled with thick pillow lavas and reworked deposits, appears bordered by two main structural highs: an articulate carbonate-pelagic platform with a stepped fault margin, and the flank of a structural high, where the volcanoclastic deposits are interlayered with reworked reef materials, suggest the occurrence of a submarine volcano, that evolved into an atoll-type carbonate shelf setting. Tectonic and magmatic events punctuated the sedimentary evolution during the Early Jurassic, Middle-Late Jurassic, Early and Late Cretaceous. The horst and graben structures connected by steeped margins and the occurrence of distinctive types of volcanic products suggest that the study areas could represent a sector of the Jurassic-Cretaceous southern Tethyan passive continental margin, situated at the edge of the continental platform bordering those basinal areas where rifting and possible spreading processes were active during the Mesozoic.

The assembly of the Gondwana supercontinent during the waning stages of the Proterozoic provides a tectonic backdrop for the myriad biological, climatological, tectonic and geochemical changes leading up to, and including, the Cambrian radiation. A polyphase assembly of Gondwana during the East Africa, Brasiliano, Kuungan and Damaran orogenies resulted in an extensive mountain chain which delivered nutrients into a shifting oceanic realm. An analysis of key evolutionary events during this time period reveals the following (a) several fauna show well established endemism that may be rooted in a cryptic evolutionary pulse (c). 580 Ma (b) the margins of the Mirovian and Mawson Oceans formed the locus of radiation for the Ediacaran fauna (c) the margins of the Iapetan and Mirovian oceans form the olenellid trilobite realm (d) the margins of the Mawson and Paleo-Asian oceans are the birthplace of the so-called Gondwana Province fauna (e) evolutionary events associated with the Cambrian radiation were likely driven by internal (biological) changes, but radiation was enhanced and ecosystems became more complex because of the geochemical, ecological and tectonic changes occurring during Ediacaran-Cambrian periods.

The estimation of human population size during the Pleistocene is complex, and one which has been dealt with extensively in the literature. However, because many of these previous estimations are based in part on archaeological site distributions, they are more a reflection of present-day geography than of what the Earth looked like in the past. We address this issue by calculating an estimation of habitable land area during the Last Glacial Maximum (between 22 and 19 kya) when sea level was 120 m lower than today using the polygon creation function in Google Earth. We then subtract areas of land that were likely uninhabitable during the LGM – either due to glacier cover, extreme aridity, elevation, or areas at high latitudes. From this, the combined habitable land areas of Eurasia, Africa and the Australian landmass are estimated as 76,959,712.4 km2. This estimation is then coupled with population density data for medium-to large-bodied carnivores, and ethnographic population density data for hunter–gatherers culled from the literature. Total human census population size in the Old World during the Last Glacial Maximum is estimated at 2,117,000–2,955,000 based on carnivore densities and 3,046,000–8,307,000 for hunter–gatherer densities.

This Atlas of Devonian Paleogeographic Maps shows the changing paleogeography from the Lochkovian (413.6 Ma) to the Devono-Carboniferous Boundary (359.2 Ma).  The maps are from volume 4 of the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2014). Absolute age assignments are from Gradstein, Ogg & Smith (2008).  An additional map showing the disposition of the three major early Devonian faunal provinces (Malvinokaffric, Appalachian, and Rhenish-Bohemian; Cocks & Torsvik, 2002; Figure 9.) has also been included.
The following maps are included in the Atlas of Devonian Paleogeographic Maps:

Map 65  Devono-Carboniferous Boundary (359.2 Ma) Transgressive Systems Track
Map 66  Late Devonian (early Famennian, 370.3 Ma) Tournasian Supersequence Boundary 
Map 67  Late Devonian (Frasnian, 379.9 Ma) Maximum Flooding Surface
Map 68  Middle Devonian (Givetian,388.2 Ma) Frasnian Supersequence Boundary
Map 69  Middle Devonian (Eifelian, 394.3 Ma) Transgressive Systems Tract
Map 70  Early Devonian (Emsian, 402.3 Ma) Maximum Flooding Surface
Map 71  Early Devonian (Pragian, 409.1 Ma) Emsian Supersequence Boundary
Map 72  Early Devonian (Lochkovian, 413.6 Ma) Lochkovian Supersequence Boundary
Extra Map – Early Devonian Biogeography

This atlas contains an “extra” map that shows the geographic distribution of three imp0ortant early Devonian biogeographic provinces: The Appalachian Province, the Rhenish-Bpohmeian Province, and the Malvino-Kaffric Province.  The Appalachian and Rhenish-Bohemian provinces were populated by warm-water brachiopod faunas the occupied the subtropics. Though they inhabited the same latitudinal zones, they were separated by the Caledonian-Acadian mountain ranges.  It is interesting to note that Appalachian faunas appear both in the Applachina Basin of the eastern U.S. and also in northern South America (Colombia and the Amazon Basin).  Similarly, the Rhenish-Bohemian faunas are found in Northern Africa, Arabia, Central Europe, and eastern Avalonia (northern France, Belgium, and southern England). The less diverse Malvino-Kaffirc province occupied cooler latitudes closer to the South Pole.

The geographic distribution of these distinct, early Devonian faunal provices provides an important clue regarding the relative positions of Laurentia (North America), Baltic and Gondwana.  Eastern North America was adjacent to northern South America (Venezuela & Colombia) and England and Central Europe were separated by a narrow ocean from northern Africa. The South Pole was located in the vicinity of southern Brazil.

This work should be cited as
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.

2013.33 These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear, or plate caree map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

A set of seven atlases has been compiled for each of the principal climatic variables: Temperature (Scotese and Moore, 2014a), Atmospheric Pressure and Winds (Scotese and Moore, 2014b),  Rainfall and Runoff (Scotese and Moore, 2014c), Ocean Currents and Salinity (Scotese & Moore, 2014d), Upwelling (Scotese and Moore, 2014e), Anoxia (Scotese, 2014b), and Lithologic Indicators of Climate (Scotese, Boucot and Xu, 2014).  These atlases show the FOAM simulation results for all 18 time intervals (Figure 1).

(More discussion about the maps in this folio in the near future.)

This map folio should be referenced as:
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.

2013.47 These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear, or plate caree map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

This "flipbook", which illustrates the plate tectonic development of the continents and ocean basins during the past 750 million years, was assembled to commemorate the scientific career of Professor Rob van der Voo.  The flipbook consists of 34 plate tectonic reconstructions that map the past location of subduction zones (barbed lines), mid-ocean ridges, (dashed lines), and collision zones (marked x's). The tectonic reconstructions are based on the global plate tectonic model developed by the PALEOMAP Project. 
The latitudinal orientation of the continents is derived largely from paleomagnetic data collected by Professor van der Voo (xref).  Hot spots tracks and sea floor spreading isochrons (Seton et al., 2012) were used to constrain the longitudinal position of the continents back to  ~200 million years.  Plate tectonic reconstructions older than 200 million years are necessarily more speculative and have been derived by combining diverse lines of evidence from the tectonic histories of the continents (e.g., timing of continent-continent collisions or ages of rifting), the distribution of paleoclimatic indicators (i.e coals, tillites, salt deposits, and bauxites, see Boucot et al., 2013), and in some case, the biogeographic affinities of fossil faunas and floras.
Though a diverse data has been used to produce these reconstructions, this data, itself, is not  enough.  So much time has passed and so little direct evidence is preserved that guidance must also be sought from the "Rules of Plate Tectonics".
Plates do not move randomly but evolve in a manner that is consistent with the forces that drive them.  The principal driving forces are: slab pull, ridge push and trench rollback.  These forces shape the plates and provide important insights into how plate boundaries will evolve.  Simply said, plates will only move if they are pulled by a subducting slab or pushed by the forces exerted by a mature ridge system. The evolving plate boundaries have been drawn to follow this maxim.  It is also important to note that plate tectonics is a "catastrophic" system.  Though "slow and steady" is the general rule, once every hundred million years or so, a major plate tectonic reorganization occurs. These "plate tectonic catastrophes" most often occur when mid-ocean ridges are subducted or when major continents collide. (For a more complete listing of the "Rules of Plate Tectonics", the reader is referred to XXXXXX.
The first "continental drift" flipbook was pushed as an undergraduate research project (Scotese, 1974; 1975abc). Subsequent editions have followed (1976ab; 1978; 1979; 1980;  1990, 1991, 1997, 2004). A more complete description of the data and information that is used to produce the flipbooks can be found in Scotese (2004).  These maps could not have been produced without the GPlates plate modelling software and the tectonic data sets published by Dietmar Müller and his team at Earthbytes.
Special thanks to Maggie Geiger, and Robert and Jonathan Scotese for their help assembling this flipbook.

Time Scale
The age given next to each map represents age in millions of years.  The corresponding geological ages (Ogg et al., 2008)  are:
0    Modern World
20 Ma  Early Miocene
40 Ma  late Middle Eocene
60 Ma  Paleocene
80 Ma  Late Cretaceous - Campanian
100 Ma  Early Cretaceous - late Albian
120 Ma  Early Cretaceous - early Aptian
140 Ma  Early Cretaceous - Berriasian
160 Ma  Late Jurassic - Oxfordian
180 Ma  Early Jurassic - Toarcian
200 Ma  Triassic/Jurassic boundary
220 Ma  Late Triassic - Carnian
240 Ma  Middle Triassic - Anisian
260 Ma  Middle Permian - Capitanian
280 Ma  Early Permian - Artinskian
300 Ma  Late Pennsylvanian
320 Ma  Late Mississippian
340 Ma  Middle Mississippian
360 Ma  Devono-Carboniferous
380 Ma  Late Devonian - Frasnian
400 Ma  Early Devonian - Emsian
420 Ma  Late Silurian - Ludlow
440 Ma  Early Silurian - Llandovery
460 Ma  Middle Ordovician
480 Ma  Early Ordovician
500 Ma  Late Cambrian
520 Ma  Middle Cambrian
540 Ma  Cambrian-Precambrian
560 Ma  Neoproterozoic - lt. Ediacaran
600 Ma  Neoporterozoic - m. Ediacaran
630 Ma  Neoproterozoic - e. Ediacaran
660 Ma  Neoproterozoic - e. Ediacaran
690 Ma  Neoproterozoic - lt. Cryogenian
720 Ma  m. Cryogenian
750 Ma  m. Cryogenian


References Cited

Ogg, J., Ogg, G., and Gradstein, F.M., 2008. The Concise Geologic Time Scale, Cambridge University Press, 177 p.
Scotese, C.R. 1974. First Flip Book Images (from 35mm film from PLATO System), Unpublished.
Scotese, C.R., and Baker, D.W., 1975a. Continental drift reconstructions and animation, Journal of Geological Education, 23: 167-171.
Scotese, C.R., 1975b.  Continental Drift Flip Book, 1stedition.Chicago, Illinois. (single page version

Scotese, C.R., 1975c.  Continental Drift Flip Book, 1st edition. Chicago, Illinois. (double page version)
Scotese, C.R., 1976a. Continental
Drift “Flip Book”,  edition 1.5, Department of Geological Sciences, University of Illinois. ResearchGate  Academia
Scotese, C.R., 1976b. A continental drift “flip book", Computers & Geosciences, 2:113-116.
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.
Scotese, C.R., 1979. Continental Drift (flip book), 2nd edition.
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.
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.
Scotese, C.R., 1991. Continental Drift Flip Book, 4th edition, PALEOMAP Project, Arlington, TX, 49 pp.
Scotese, C.R., 1997.  Continental Drift Flip Book, 7th edition, PALEOMAP Project, Department of Geology, University of Texas at Arlington, Texas, 80 pp.

Scotese, 2004.
Seton et al., 2012.
Van der Voo,  R., 1993. Paleomagnetism of the Atlantic, Tethys, and Iapetus Oceans, Cambridge University Press, 411 p.

This map folio should be referenced as:
Scotese, C.R., 2013. Map Folio 86, Middle Cambrian, (520 Ma), PALEOMAP PaleoAtlas for ArcGIS, volume 5, Early Paleozoic Paleogeographic, Paleoclimatic and Plate Tectonic Reconstructions, PALEOMAP Project, Evanston, IL.
Also see: 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, https://www.academia.edu/16785571/Atlas_of_Cambrian_and_Early_Ordovician_Paleogeographic_Maps

Introduction
These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear map projection can also be directly “wrapped” onto a spherical projection, like the one used by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

ViUeneuve, M., 1989. The geology of the Madina-Kouta basin (Guinea-Senegal) and its significance for the geodynamic evolution of the western part of the West African Craton during the Upper Proterozoic period. Precambrian Res., 44: 305-322. The Madina-Kouta basin is a southward extension of the upper Proterozoic Taoudeni basin. This sedimentary basin formed in a SW-NE tectonic fault zone in the Leo shield at ~ 1000-800 Ma. The deposits indicate a quiet and slightly subsiding area. An important uncofformity allows us to distinguish two lithostratigraphic groups: the Sdgou Group below and the Madina-Kouta Group above. Sedimentation in this area ended with the Late Proterozoic glaciation 650-620 Ma. The correlations with the Taoudeni basin show a close relationship between the foreland area and the Mauritanides/ Bassarides fold belt during the Pan-African I cycle (800-650 Ma). In particular we suppose that the lower part of the Taoudeni basin deposits which correlate with the Madina-Kouta Group (group of Souroukouto) is on the passive margin of the Pan-African I rift, and the post-Madina-Kouta deposits in the Taouc]~ni basin (Group of Bakoye) correspond to the molassic stage of the Pan-African I fold belt (rift closure stage).

2014.10 This Atlas of Early Cretaceous Paleogeographic Maps shows the changing paleogeography from the Berriasian (143 Ma) to the late Albian (101.8 Ma).  The maps are from volume 2 of the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2014).
Also numeric time values are from Gradstein, Ogg & Smith (2008).  For several stages there are versions of the map that show maximum sea level (maximum flooding surface) or minimum sea level (supersequence boundary) during that time interval.

The following maps are included in the Atlas of Early Cretaceous Paleogeographic Maps:

Map 23  Early Cretaceous (late Albian, 101.8 Ma)
Map 24  Early Cretaceous (middle Albian, 106 Ma)
Map 25  Early Cretaceous (early Albian, 110 Ma)  Albian Supersequence Boundary and Transgressive System Tract
Map 26  Early Cretaceous (late Aptian, 115.2 Ma)
Map 27  Early Cretaceous (early Aptian, 121.8 Ma)
Map 28  Early Cretaceous (Barremian, 127.5 Ma)
Map 29  Early Cretaceous (Hauterivian, 132 Ma)
Map 30  Early Cretaceous (Valanginian, 137 Ma) Barremian-Hauterivian Supersequence boundary and Transgressive Systems Tract
Map 31  Early Cretaceous (Berriasian, 143 Ma) Berriasian Supersequence boundary and Maximum Flooding Surface

This work should be cited as
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.

Computerized evaluation of Vibroseis similarity test data is the logical consequence of the increasing quality requirements for signal reproducibility and for synchronization of vibrators. The differences in start time and phase as well as an indication of local phasing problems between any two Vibroseis signals can be obtained from an analysis of the difference of their respective phase spectra. This method appears to be accurate and stable with respect to harmonics which usually plague the signals from transducers monitoring the motion of the vibrators'base plates.

Plusieurs études multidisciplinaires ont été effectuées sur les couches riches en matière organique (MO) de la Formation Bahloul. Nos études de terrain et les synthèses géologiques, géochimiques, isotopiques et minéralogiques disponibles ont permis d'apporter des précisions nouvelles d'ordre paléogéographique et paléocéanographique. Ces données ont contribué à l'élaboration d'un modèle de dépôt sous une zone à minimum d'oxygène (ZMO) dans des bassins marins profonds et subsidents de type bathyal, où se sont accumulées et préservées d'importantes quantités de MO (jusqu'à 18,7 % de COT). Le présent modèle a permis la corrélation de la Formation Bahloul à d'autres coupes de référence à l'échelle globale, ce qui permet de mettre en évidence que le d 13 C mesuré sur MO serait un meilleur outil de corrélation que le d 13 C mesuré sur carbonates pour reconnaître la limite Cénomanien/Turonien. Mots clés Formation Bahloul ; Géochimie ; Stratigraphie ; EAO-2 ; Cénomanien-Turonien ; matière organique; modèle de dépôt.

2013.41 These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear, or plate caree map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com.

The Marajó Basin area presents geologic and geomorphologic features chiefly due to the Mesozoic extension and post-Miocene neotectonics. The extension event with an Early and a Late Cretaceous phases originated four sub-basins that constitutes the Marajó Basin, with a thick continental clastic sequence showing marine influence. NW and NNW normal faults and NE and ENE strike-slip faults controlled the basin geometry. The extension, related to the Equatorial Atlantic opening, propagated into the continent along crustal weakness zones of the Precambrian Tumucumaque, Amapá and Araguaia orogenic belts. The neotectonic event is a strike-slip regime which developed transtensional basins filled in by Upper Tertiary shallow marine (Pirabas Formation) and transitional sequences (Barreiras Group), followed by Quaternary fluvial deposits and transitional sequences derived from the Amazon and Tocantins rivers and the Marajoara estuary. The current landscape has a typical estuarine morphology. The coast morphology presents sea-cliffs on transitional Upper Tertiary sequences, while inwards dominate hills sustained by Mid-Pleistocene lateritic crust, with a flat erosive surface at 70 m. In the eastern Marajó Island several generations of paleochannels associated with fluvial-estuarine sequences are recognized, while a fluvial-marine plain is widespread on its western side.

Ferrari et al. [Ferrari, O.M., Hochard, C., Stampfli, G.M., 2008. An alternative plate tectonic model for the Palaeozoic–Early Mesozoic Palaeotethyan evolution of Southeast Asia (Northern Thailand–Burma). Tectonophysics 451, 346–365. doi:10.1016/j.tecto.2007.11.065.] redefine the “Shan-Thai” terrane in Thailand as a Cathaysian Indochina-derived terrane when this has traditionally been defined and used as a Gondwana-derived continental block, hence introducing unnecessary confusion. In their definition of “Shan-Thai”, they also inappropriately combine oceanic suture zone rocks (the Palaeo-Tethys Inthanon suture) and continental arc rocks (Sukhothai Island Arc system). TheMai YuamFault, identified by Ferrari et al. (2008) as the Palaeo-Tethys suture, is in fact a Cenozoic fault and the Palaeo-Tethys suture zone is represented by the Inthanon Suture zone in Thailand which is equivalent to the previously recognised Inthanon zone. The concept of derivation of “Orang Laut” terranes from South China-Indochina by back-arc spreading is innovative but the proposed Permo-Triassic back-arc along the Song Da/Song Ma zone in Vietnam is less convincing. There is little evidence to support the proposed southwards subduction of Palaeo-Tethys beneath eastern Gondwana in the Permian.

2013.17 These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear, or plate caree map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

Seu conteúdo foi revisado pelo Comitê Técnico do IV SimBGf, mas não necessariamente representa a opinião da SBGf ou de seus associados. É proibida a reprodução total ou parcial deste material para propósitos comerciais sem prévia autorização da SBGf.

2014.07 This Atlas of Neogene Paleogeographic Maps shows the changing paleogeography from the Early Miocene (Auquitanian & Burdigalian, 19.5 Ma) to the Present-day.  The maps are from volume 1 of the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2014). Absolute age assignments are from Ogg, Ogg & Gradstein (2008).

For Maps 3, 5 and 7, there are two versions of the paleogeography. One map shows the maximum highstand sea level (maximum flooding surface). The other map shows the minimum lowstand sea level (supersequence boundary). For each paleogeography there is an estimate of sea level change, in meters, relative to present-day sea level. 

The following maps are included in the Atlas of Neogene Paleogeographic Maps:

Map 01  Modern World (Holocene, 0.0 Ma) Transgressive Systems Tract
Map 02  Last Glacial Maximum (Pleistocene, 21,000 years ago) Anthropocene Supersequence Boundary 
Map 03  Plio-Pleistocene, (Gelasian & Piacenzian, 2.588 Ma Ma) Lowstand Systems Tract
Map 04  Latest Miocene (Messinian Event, 6.3 Ma) Maximum Flooding Surface
Map 05  Middle/Late Miocene, (Serravallian and Tortonian, 10.5 Ma) Messinian Supersequence Boundary & Tortonian Maximum Flooding Surface
Map 06  Middle Miocene (Langhian, 14.9 Ma) Maximum Flooding Surface
Map 07  Early Miocene (Aquitanian & Burdigalian, 19.5 Ma) Serravallian Supersequence Boundary, Aquitanian Maximum Flooding Surface

This Atlas should be cited as:
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.



References Cited

Ogg, J.G., Ogg, G., Gradstein, F.M., 2008. The Concise Geologic Time Scale, Cambridge University Press, Cambridge, UK, 177 pp.

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, Evanston, IL.

This monograph begins with a brief review of the most important foraminiferal zonations, and the late Devonian-early Carboniferous foraminiferal zonation in Moravia where some key profiles allow a good correlation with the conodont zonation. In the late Devonian-early Carboniferous, fourteen
foraminiferal zones· are precisely defined in Moravia and correlated with other important foraminiferal zonations in all the paleobiogeographic realms and with zonations based on other groups of fauna (corals, stromatoporoids, conodonts, ammonoids). The correlation of foraminiferal zonations generally confirms the similar development of foraminiferal faunas in Western and Eastern Europe. Certain difficulties were encountered when different index species and taxonomic
approaches have been used (in the middle-late Visean and some differences were observed in the early and late Tournaisian. Correlations between different  aleobiogeographic realms of the Northern Hemisphere are more difficult and less exact, their precision varying over time. The best correlations are in the late Frasnian, the late Famennian, the late Tournaisian, and the late Visean, when a considerable similarity of foraminiferal faunas is observed. The poorest correlations are in the lower part of the Famennian, Tournaisian and Visean, when foraminiferal faunas of both the Siberian and North American realms are considerably depleted in comparison with the North Paleotethyan Realm.
When comparing foraminiferal zonation with other benthic fauna zonations from the point of view of biostratigraphical resolution, we can see that the Famennian foraminiferal zonation provides the highest resolution among the benthic fauna zonations. When compared with conodont and
ammonoid zonation, the foraminiferal zonation does not reach their high levels of resolution in the late Devonian. In the middle and late Tournaisian, the stratigraphical range of conodont and foraminiferal zones is comparable and the foraminiferal zones are finer than the ammonoid zones. 'In the early and middle Visean, the foraminiferal zonation represents the most detailed subdivisions of this interval and in the late Visean, only the ammonoid zonation acquires a level of resolution similar to the foraminiferal zonation. Four freely interconnected late Devonian-early Carboniferous paleobiogeographical realms are distinguished in the paper: the tropical/subtropical _ North Paleotethyan Realm, the North American Realm, the northern boreal Siberian Realm and in accordance with Leven (Leven, 1993; Leven & Okay, 1996), the newly defined southern boreal Perigondwana Realm that includes the Central Mountains Terrane in Afghanistan, the Karakoram, the Himalayan Tethyan Zone and the higher-latitude Cimmerian Qiantang. The Baoshan, Libya (the Cyrenaica Basin) and Egypt (Western Desert, Sinai) may also be included in this latter realm. In the North Paleotethyan
Realm, the Fennosarmatian, Armorican, Central Asiatic, East Asiatic and Paleopacific (Kamchatka-Koryak, Anyut-Chukotka and Mongolo-Okhotsk fold belts) provinces are distinguished. Northwestern Africa is regarded as a part of the realm only in the upper part of the Visean. In North America, the Pacific coast and Alaska fauna are not regarded as a part of the North
American Realm. The northern temperate-to-cool Siberian Realm is composed, largely in accordance with Vdovenko (1980), of the Kuznets, Tunguska, Verkhoyansk, Chersk, Kolyma and Omolon provinces. The correlation of some Alaskan terranes with Siberian terranes is reinforced by the presence of
endemic Juferevella (known only in the Dillinger Terrane and the Kuznets Province) as well as by the presence of Quasiendothyra and Mediocris. However, Alaska represents a collage of terranes with different affinities and no uniform Alaska Province can be defined. In the present monograph, only
the Kuznets and Tunguska provinces are regarded as typical parts of the Siberian Realm. The Omolon, Omulevka, Prikolyma terranes corresponding to the Omolon, Kolyma and Chersk provinces, exhibit a strong North Paleotethyan influence during the late Devonian and the Tournaisian and only became a part of the Siberian Realm in the Visean. The Taimyr fauna, which show strong North Paleotethyan influences, has an enigmatic position. The major evolutionary events for foraminiferal fauna may be summarized in the following way: 1. A major late Frasnian diversification of multilocular forms 2. The Frasnian/Famennian exctinction 3. Low diversity in the Early Famennian 4. A Middle Famennian diversification 5. A Late Famennian diversification of Quasiendothyra fauna 6. The Devonian/Carboniferous stepwise extinction of quasiendothyrs
7. Low diversity in the Early Tournaisian 8. A Middle Tournaisian diversification of Chernyshinella fauna 9. The Middle/Late Tournaisian decline of chernyshinells 10. A Late Tournaisian diversification of Kizel and Kosvin fauna 11. The Visean diversification reaching its acme in the late ViseanThe evolution of foraminiferal fauna was closely connected with climatic oscillations and it seems tempting to adopt the idea that glaciation in Gondwana was one of the triggering factors of the foraminiferal migrations and paleobiogeography. The pattern of climatic oscillations seems to represent a certain cyclic trend within the late Devonian and early Carboniferous. The upper part of the stages (late Frasnian, late Famennian,
late Tournaisian, late Visean) may always be regarded as thermal periods, the lower part of the stages being "glacial" periods. Similar to the situation at the Cretaceous/Tertiary boundary, we can also see a major loss of the tropical temperature sensitive biotas and a small impact on the temperate/eurytopic biotas at the Frasnian/Famennian and Devonian/ Carboniferous boundaries. Even though glaciation in Gondwana may have existed over the whole of the late Devonian-early Carboniferous interval, the cyclic nature of the climate allowed even intertropical fauna occasionally to reach sub-polar areas during temperate climatic phases. The impact of foraminiferal paleobiogeography on plate tectonic reconstructions at the southeastern margin of Laurussia and in southwestern Asia is discussed. The Brunovistulian, Moesian, Zonguldak and Istanbul terranes in Central and southeastern Europe and Asia Minor (the Brunovistulian group of terranes) show close paleobiogeographic relationships to the East European foraminiferal association and are consequently regarded as a part of the Fennosarmatian Province.
The Anatolide-Tauride Zone, the Elburz and the North Afghan block constitute a group of terranes which show some features in common. The foraminiferal associations of the North Paleotethyan affinity begin here at the Tourrnaisian/Visean boundary and in this respect they compare well with the Armorican Province, including the Intra-Alpine group of terranes
(Stampfli, 1996) in the east. The foraminiferal associations show close ties to the southern margin of Laura.sia, Le. to the Fennosarmatian and/or Central Asiatic provinces and are quite different from the foraminiferal associations of other parts of the "Cimmerian Superterrane" and the southern Paleotethyan
margin (northeastern and northwestern Africa). Similar trends can also be traced in the coral fauna. The model that best fits with available evidence is that AnatolideTauride Zone was ei,ther a part of or located close to Laurasia in the Carboniferous. The Istanbul Zone represents the equivalent of the Rhehohercynian Zone of Central Europe and cannot be compared with the Intra-Alpine or south Variscan terranes, which in turn may be correlated with the Anatolide-Tau ride Zone. Later, in the Permian, the AnatolideTauride Zone may have been separated from the Eurasian mainland by the Meliata-Dobrogea-Karakaya back-arc ocean. A similar model-either a Variscan soft docking or a location close to Laurasia-is also inferred for the Elburz Terrane. In Afghanistan, the foraminiferal associations of the North Afghan Block, traditionally regarded as a part of the Variscan Zone on the northern Paleotethys margin, compare well with both the Elburz
and the Anatolide-Tauride Zone and contrast with cool water fauna of the Cimmerian Central Mountains Terrane (Perigondwana Realm).

2014.11 This Atlas of Jurassic Paleogeographic Maps shows the changing paleogeography from the Hettangian (198 Ma) to the Jurassic/Cretaceoous Boundary (145.5 Ma).  The maps are from volume 3 of the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2014). Absolute age assignments are from Gradstein, Ogg & Smith (2008). 

The following maps are included in the Atlas of Jurassic Paleogeographic Maps:

Map 32  Jurassic/Cretaceous Boundary (145.5 Ma) Berriasian Supersequence Boundary
Map 33  Late Jurassic (Tithonian, 148.2 Ma) Highstand Systems Track 
Map 34  Late Jurassic (Kimmeridgian, 153.2) Maximum Flooding Surface
Map 35  Late Jurassic (Oxfordian, 158.4) Transgressive Systems Track
Map 36  Middle Jurassic (Callovian, 164.5 Ma) Transgressive Systems Tract
Map 37  Middle Jurassic (Bajocian & Bathonian, 169.7 Ma) Kimmeridgian-Oxfordian Supersequence Boundary & Maximum Flooding Surface
Map 38  Middle Jurassic (Aalenian, 173.2 Ma) Bathonian-Bajocian Supersequence Boundary
Map 39  Early Jurassic (Toarcian, 179.3 Ma) Toarcian Supersequence Boundary and Maximum Flooding Surface
Map 40  Early Jurassic (Pliensbachian, 186.3 Ma) Maximum Flooding Surface
Map 41  Early Jurassic (Sinemurian, 193 Ma) Transgressive Systems Track
Map 42  Early Jurassic (Hettangian, 198 Ma) Pliensbachian Supersequence Boundary


This work should be cited as
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.

The encompassing aim of the European Science Foundation Programm "Environments and Ecosystem Dynamics of the Eurasian Neogene (EEDEN), is the detailed analysis of the response of terrestrial ecosystems to environmental change through the integration of multidisciplinary studies focussing on some selected, already fairly well-known "high-resolution" time intervals in the Neogene of the Eurasian realm. These intervals are known to (a) include major changes in the composition of terrestrial communities, (b) portray large-scale palaeogeographical reorganizations and changes in overall environmental conditions in the terrestrial realm and (c) allow the establishment of high-resolution stratigraphie correlations with data and interpretations pertaining to regional and global aspects of the coeval development of marine environments. They cover (1) the latest Miocene to Early Pliocene (HRI 1:7-4 Ma ago), (2) the latest Middle Miocene to early Late Miocene (HRI 2: 12 -8.5 Ma ago) and the late Early to early Middle Miocene (HRI3: 17-14 Ma ago).

2013.21 These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear, or plate caree map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

2013.53 These maps (rectilinear projection) are from the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2013a-f).  This is a digital atlas of plate tectonic, paleogeographic, and paleoclimatic reconstructions designed for use with the GIS software, ArcMap (ESRI).  Table 1 lists the various types of maps that comprise the PALEOMAP PaleoAtlas.  The maps included in this folio are highlighted in bold text (Table 1).
The last map in each folio is a rectilinear graticule that can be overlain on the maps to provide a geographic reference frame.  A rectilinear projection was used because it can be easily georeferenced in ArcMap and transformed into a variety of other map projections.  The rectilinear map projection can also be directly “wrapped” onto a spherical projection, like the oneused by Google Earth. A set of Google Earth paleoglobes has made from the maps in this folio. These Google Earth paleoglobes can be downloaded at: www.globalgeology.com. 
If the map you need is missing, or if there doesn’t seem to be a map folio for the exact time interval of interest, please contact me ([email protected]). Table 2 lists all the time intervals that comprise the PALEOMAP PaleoAtlas for ArcGIS. The PaleoAtlas contains one map for every stage in the Phanerozoic, as well as 6 maps for the late Precambrian.  Eventually, Map Folios, like this one, will be published for every time interval in the PALEOMAP PaleoAtlas.  The following section is a brief description of the maps that makeup the Map Folio.

This Atlas of Cambrian and Early Ordovician Paleogeographic Maps shows the changing paleogeography from the base of the Cambrian (542 Ma) to the Early Ordovician (Arenig, 473.4 Ma).  The maps are from volume 5 of the PALEOMAP PaleoAtlas for ArcGIS (Scotese, 2014). Absolute age assignments are from Gradstein, Ogg & Smith (2008). 

The following maps are included in the Atlas of Cambrian and Early Ordovician Paleogeographic Maps:

Map 81  Early Ordovician (Arenig, 472.4 Ma) Arenigian Supersequence Boundary
Map 82  Early Ordovician (Tremadoc, 480 Ma) Maximum Flooding Surface 
Map 83  Cambro-Ordovician Boundary (488.3 Ma) Tremadocian Supersequence Boundary
Map 84  Late Cambrian (Furongian, 494 Ma) Croixian Supersequence Boundary
Map 85  early Late Cambrian (510 Ma) Transgressive Systems Tract
Map 86  Middle Cambrian (520 Ma) Transgressive Systems Tract
Map 87  Early Cambrian (531.5 Ma) Albertan Supersequence Boundary
Map 88  Cambrian-Precambrian Boundary (542 Ma) Caerfaian Supersequence Boundary


This work should be cited as
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.

The position of the central axis of deposition over Colombian and Venezuelan continental crust has varied markedly through time. The axis migrated from west to east from Late Cretaceous to Oligocene but at times, secondary drainage divides were established by local uplift events. In Oligocene times with initial inversion of the Eastern Cordillera the central axis of deposition was divided into two main axes, the proto-Magdalena and the proto-Orinoco systems. The west to east migration of the central axis of deposition had a tectonic origin and it occurred in combination with tectonically driven changes in accommodation space. Depocenter evolution can be divided as follows. (1) The axis of the Campanian and early Maastrichtian depocenter was located few km east of the present position of the Central Cordillera of Colombia; it migrated east with gradual uplift of the Central Cordillera. (2) The central axis of late Maastrichtian deposition is positioned approximately over the present-day western foothills of the Eastern Cordillera, possibly crosses the Eastern Cordillera over the Santander Massif and continues into the Maracaibo Lake in western Venezuela. Accommodation space decreased from Campanian to Maastrichtian times. In Cretaceous-Tertiary boundary times parts of the eastern margin of the Eastern Cordillera were uplifted by an initial phase of inversion of deeply rooted Jurassic and Early Cretaceous normal faults. (3) In Paleocene times the central axis of deposition was located along the spine of the Eastern Cordillera and extended into the Maracaibo Basin, and accommodation space continued to decrease. (4) In latest Paleocene times the central axis of deposition shifted to eastern regions of the Eastern Cordillera and accommodation space decreased. The Early Eocene central axis of deposition was located along the present-day eastern foothills of the Eastern Cordillera; accommodation space continued to decrease and the regional Middle Eocene unconformity began to develop. In Middle Eocene times a regional unconformity developed, marking the climax of the pre-Andean Orogeny. Deposition during these times was dominant in the Maracaibo Basin area where large amounts of sediment derived from vast exposed areas accumulated. (6) The Late Eocene central axis of deposition was confined to the present position of the Llanos foothills. Late Eocene deposition reflects a regional increase in accommodation space. In Oligocene times the initial uplift of the Eastern Cordillera divided the main depocenter into two central axes. Accommodation space diminished in uplifted regions but continued to increase in the depocenters allowing sporadic marine ingressions into the present position of the Llanos foothills. As uplift of the Eastern Cordillera continued, the eastern depocenter axis (proto-Orinoco) migrated east and the western depocenter axis (proto-Magdalena) migrated west. This process continued through the rest of the Cenozoic. : S 0 0 3 1 -0 1 8 2 ( 9 9 ) 0 0 0 7 5 -9

This paper presents the archaeobotanical and archaeozoological data of the 6th to 4th millennia cal BC sequence recently documented at Dehesilla Cave, and puts forward an interdisciplinary approach to the significant ecological patterns from this key archaeological site in the Southern Iberian Peninsula throughout the entire Neolithic period. Results indicate an ecological scenario characterised mainly by oak and wild olive forests, and human populations with agricultural practices and herds of mainly sheep and goats. However, this general panorama must have undergone several remarkable fluctuations. The first Neolithic populations of Dehesilla Cave, dated around the mid-6th millennium cal BC and linked to the Mediterranean impressa pottery complex, do not yet display evidences of agriculture, while all of the subsequent Early Neolithic levels indicate a model of small-scale populations with a mixed economy but still with a greater component of livestock. The second quarter of the 5th millennium cal BC shows a marked accentuation of the monoculture of naked wheats, which could have been related to the transition from an intensive to an extensive farming system. This may have entailed a selective pressure on the environment, leading to a large deforestation spanning the second half of the 5th millennium cal BC and the constitution of relatively open thermo-Mediterranean forests with a physiognomy similar to that of the dehesa. These ecological patterns are discussed within a review of the current state of the art of the use of plant and animal resources by the Neolithic human populations in the southern regions of the Iberian Peninsula.

The aim of this study is to determine the environmental changes around the Beytitepe (Tepetarla) mound in the Holocene and to evaluate human-environment relationships. With regard to the paleogeography and geoarchaeology of the mound, a great number of sediment samples obtained from core drillings were analised. By means of the element analysis using ICP, AAS, SFM and KJELDAHL devices, different sediment units and their environments in the Ödemiş plain, which is in the inner part of Küçük Menderes graben in the Western Anatolia, were defined and differenciated. Detailed analyses also provided to identify some paleosol deposits. Thus, archaeological deposits, fire remains, burned soil material, river sediments, wetland or swamp sediments and their peat-like materials can be distinguished in the Bronze Age settlement of Beytitepe mound and its surroundings. In this study, a simple stratigraphic model is defined for the Bronze Age mounds of Ödemiş plain, and by means of paleogeographical-geoarchaeological interpretations, significant contributions were provided to the archaeology of the Beytitepe mound. Öz Bu çalışmanın amacı, Küçük Menderes havzası içindeki Ödemiş ovasının tabanında bulunan Beytitepe (Tepetarla) höyüğü çevresinde Holosen'de meydana gelen doğal çevre değişmelerinin belirlenmesi ve insan-çevre ilişkilerinin değerlendirilmesidir. Höyük çevresinin paleocoğrafya ve jeoarkeolojisinin ele alındığı bu çalışmada höyük ve çevresinde yapılan sondajlardan alınan sediman örneklerinin değerlendirilmesinde element analizlerinden yararlanılmıştır. ICP, AAS, SFM ve KJELDAHL cihazları kullanılarak yapılan element analizleri ile Batı Anadolu'da, Küçük Menderes grabeninin iç kesiminde bulunan Ödemiş ovasının farklı sediman katmanlarının ayırt edilmesine ve ortamlarının belirlenmesine çalışılmıştır. Detaylı analizlerin sonucunda paleosol katmanlarının tespiti üzerinde de durulmuştur. Bu analizlerin yardımı ile Tunç Çağı yerleşimi olan Beytitepe höyüğünün