Paleozoic

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 (cscotese@gmail.com). 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.

In central Utah, the major pre-Mississippian unconformity is fairly well understood at most of the localities where it is recognized. However, the unconformity is more enigmatic in Rock Canyon of the central Wasatch Range. At this locality, dolomitization of most pre-Mississippian rocks obscures stratigraphic identification of Devonian and older units. The absence of any identifiable angular relationship further complicates resolution. Because of this, both identification of the stratigraphic level of the unconformity and, consequently, its magnitude remain controversial. Large-size dolomite samples taken in Rock Canyon at closely spaced intervals for the 3.6-m directly below definite Upper Devonian rocks yield microfossils, including conodonts, in the uppermost 1.6-m of that interval that indicate no unconformity exists between the Cambrian Maxfield Limestone and the Upper Devonian-Lower Mississippian Fitchville Dolomite at the horizon previously identified as unconformable. Rather, an unknown thickness of dolomitized Upper Devonian Pinyon Peak Formation and probable older rock (possibly Bluebell Dolomite and Victoria Formation) occurs between the top of definite Maxfield and base of the
Fitchville. The identification of the unconformity horizon remains unknown. Our preliminary work outlines a promising procedure for future understanding of the magnitude and stratigraphic level of
the unconformity.

A number of motored auger holes have been drilled in 2002 and 2006 in four sand-clay deposits preserved in dissolution pockets within the Dinantian limestones of the watershed north of the Vesdre valley. These deposits of unknown age are currently classified as (Tertiary) SBL in the new geological map of Wallonia. We present detailed lithostratigraphic logs of the deposits and describe the results of sedimentological and mineralogical analyses. In particular, K-Ar dating of neoformed Mn oxides found at the base of one augerhole at Rechain yielded ages ranging from Cenomanian to Santonian, allowing us to place the Rechain and Andrimont deposits within the early Late Cretaceous. This is fully consistent with their topographic location very close beneath the trace of the pre-Cretaceous erosion surface and makes them the westernmost remains of the Hergenrath Member of the Late Cretaceous Aachen Formation. To the west, the Magnee deposit is more "typical SBL", probably correspo...

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.

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 (cscotese@gmail.com). 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.

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 (cscotese@gmail.com). 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.

En la provincia geológica de Ventania, la unidad orográfica denominada Sierras Australes, ubicada al sector sureste de la provincia de Buenos Aires, se desarrolla como una cadena montañosa formando cordones subparalelos que alcanzan los 180 kilómetros de longitud en dirección NO a SE y 50 kilómetros de ancho en su parte central. Al noroeste, comienza con las Sierras de Puán y de Pigüé, expresándose ya en esta ultima el valle central que, en la región central del arco, separa las Sierras de Curamalal (al Oeste) y de Bravard (al Este) (José Sellés Martínez, 2001). En tanto el sector oriental del sistema de Ventania se encuentra formado por las Sierras de las Tunas y de Pillahuincó (Harrington, 1947). En su extremo noroeste, las sierras presentan una
flexura cóncava hacia el oeste, dando una configuración general arqueada. En dicha ubicación (Figura 1) fue realizado el trabajo de campo, focalizado en las sierras de Bravard y Curamalal.

Las rocas presentes en las Sierras Australes fueron depositadas en una extensa cuenca paleozoica desarrollada en el margen del Gondwana, deformada a principios del Mesozoico, y posteriormente exhumada por procesos extensivos mesozoicos, generando a su vez asomos aislados del basamento regional, compuesto de rocas graníticas y riolíticas milonitizadas (Harrington, 1947).

_______________________________________________________________________________________

Geomorphological Analysis of the Bravard and Curamalal Sierras, Buenos Aires Province, 2019
In the geological province of Ventania, the orographic unit called Sierras Australes, located in the southeastern sector of the province of Buenos Aires, develops as a mountain chain forming sub-parallel cords that reach 180 kilometers in length in a NW to SE direction and 50 kilometers from wide in its central part. To the northwest, it begins with the Sierras de Puán and Pigüé, expressing itself in the latter the central valley that, in the central region of the arch, separates the Sierras de Curamalal (to the West) and Bravard (to the East) (José Sellés Martínez , 2001). While the eastern sector of the Ventania system is formed by the Sierras de las Tunas and Pillahuincó (Harrington, 1947). In its extreme northwest, the mountains present a
concave flexure to the west, giving a general arched configuration. In this location (Figure 1) the field work was carried out, focused on the Bravard and Curamalal mountain ranges.

The rocks present in the Sierras Australes were deposited in an extensive Paleozoic basin developed on the Gondwana margin, deformed at the beginning of the Mesozoic, and later exhumed by extensive Mesozoic processes, generating in turn isolated outlines of the regional basement, composed of granitic rocks and mylonitized rhyolitics (Harrington, 1947).

Variably deformed metasedimentary rocks (interbedded metaquartzite, phyllite, slate, etc.) of Paleozoic age exposed at Kg. Kuala Abang, Terengganu, are separable into two units on the basis of discernible differences in structural features. The lower unit exhibits two phases of folding; the earlier southeasterly plunging reclined fold (F1) is refolded by a later southerly plunging upright fold (F2). The divergent axial trends indicate that the two phases of folding are not coaxial. The upper unit appears to have experienced only one phase of folding corresponding to the F2-fold of the lower unit. This is also evidenced by the marked differences in the occurrence of quartz veins in the two units. The lower unit displays two sets of quartz veins corresponding to the axial planes of Fl and F2, whereas quartz veins parallel to the F2 axial plane are only present in the upper unit. The difference in the structural features between the two units suggest that the deposition of the upper unit postdated the F1 folding phase implying the probable existence of an unconformity in the Paleozoic metasedimentary sequence. The age of this probable unconformity remains uncertain and can be resolved only when the ages of the metasediments at Kg. Kuala Abang are known.

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.

This Atlas of Permo-Carboniferous Paleogeographic Maps shows the changing paleogeography from the Early Mississippian (Tournasian, 352.3 Ma) to the Early Permian (Kungurian, 273.1 Ma).  The maps are from volume 4 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 Permo-Carboniferous Paleogeographic Maps:

Map 53  Early Permian (Kungurian, 273.1 Ma) Highstand Systems Tract
Map 54  Early Permian (Artinskian, 280 Ma) Maximum Flooding Surface 
Map 55  Early Permian (Sakmarian, 289.5 Ma) Maximum Flooding Surface
Map 56  Early Permian (Asselian, 296.8 Ma) Sakmarian Supersequence Boundary & Maximum Flooding Surface
Map 57  Late Pennsylvanian (Gzhelian, 301.2 Ma) Asselian Supersequence Boundary & Maximum Flooding Surface
Map 58  Late Pennsylvanian (Kasimovian, 305.3 Ma) Maximum Flooding Surface
Map 59  Middle Pennsylvanian (Moscovian, 309.5) Transgressive Systems Tract
Map 60  Early Pennsylvanian (Bashkirian, 314.9 Ma) Bashkirian Supersequence Boundary & Maximum Flooding Surface
Map 61  Late Mississippian (Serpukhovian, 323.2 Ma) Maximum Flooding Surface
Map 62  Middle Mississippian (late Visean, 332.5 Ma) Highstand Systems Tract
Map 63  Middle Mississippian (early Visean, 341.1 Ma) Maximum Flooding Surface
Map 64  Early Mississippian (Tournasian, 352.3 Ma) Maximum Flooding Surface


This work should be cited as
Scotese,  C.R., 2014.  Atlas of Permo-Carboniferous Paleogeographic Maps (Mollweide Projection), Maps 53 – 64, Volumes 4, The Late Paleozoic, PALEOMAP Atlas for ArcGIS, PALEOMAP Project, Evanston, IL.

This map folio should be referenced as:
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.
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 (cscotese@gmail.com). 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 Silurian and Middle-Late Ordovician Paleogeographic Maps shows the changing paleogeography from the Middle Ordovician (Darwillian, 464.5 Ma) to the Late Silurian (Ludlow & Prodoli, 419.5 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 Silurian and Middle-Late Ordovician Paleogeographic Maps:

Map 73  Late Silurian (Ludlow & Pridoli, 419.5 Ma) Lochkovian Supersequence Boundary
Map 74  Middle Silurian (Wenlock, 425.6 Ma) Highstand System Tract 
Map 75  Early Silurian (late Llandovery, 432.1 Ma) Maximum Flooding Surface
Map 76  Early Silurian (early Llandovery, 439.8 Ma) Transgressive Systems Tract
Map 77  Late Ordovician (Hirnantian, 444.7 Ma) Llandoverian Supersequence Boundary
Map 78  Late Ordovician (Ashgill, 448.3 Ma) Lowstand Systems Tract & Maximum Flooding Surface
Map 79  Late Ordovician (Caradoc, 456 Ma) Maximum Flooding Surface
Map 80  Middle Ordovician (Darwillian, 464.5 Ma) Llandeilian Supersequence Boundary


This work should be cited as
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.

Various red, black and grey 'Belgian marbles' (coloured dense fossiliferous Palaeozoic limestones suitable for polishing - 'calcaires marbriers') decorated private and public buildings as well as sanctuaries within and beyond the civitas Tungrorum. These hard limestones have all been quarried in southern Belgium, at the heart of the civitas. For their transport, trade and distribution, fluvial routes were most probably used. The 'Belgian marbles' have been employed as tesserae in mosaics, opus sectile, marble veneers and various smooth or sculptured wall and floor decorative elements. The strongly veined Gris des Ardennes and the wild cherry-red Rouge de Rance were the most popular ones, whereas the spotles black de Namur 'marble' was preferentially used in floor mosaics in combination with white tesserae.  The grey Meuse limestone was the most commonly used decorative stone showing a broad spectrum of applications. In this paper, the geographical-geological provenances and stratigraphical assignments of the 'Belgian marbles' (and related limestones) are discussed, whereas an overview is given of their major macroscopical-microscopical characteristics and known distribution.

Roman Ornamental Stones in North-Western Europe. Natural Resources, Manufacturing, Supply, Life & After-Life, Coquelet C., Creemers G., Dreesen R. & Goemaere E. (Eds.), Proceedings of the International Conference 'Roman Ornamental Stones in North-Western Europe, Tongeren', 20-22 April 2016. Available in the museum's shop.

The renowned soft-bodied faunas of the Cambrian period, which
include the Burgess Shale, disappear from the fossil record in the late Middle Cambrian, after which the Palaeozoic fauna dominates. The disappearance of faunas of Burgess Shale type curtails the stratigraphic record of a number of iconic Cambrian taxa. One possible explanation for this loss is a major extinction, but more probably it reflects the absence of preservation of similar softbodied faunas in later periods. Here we report the discovery of numerous diverse soft-bodied assemblages in the Lower and
Upper Fezouata Formations (Lower Ordovician) of Morocco,
which include a range of remarkable stem-group morphologies
normally considered characteristic of the Cambrian. It is clear that biotas of Burgess Shale type persisted after the Cambrian and are preserved where suitable facies occur. The Fezouata biota provides a link between the Burgess Shale communities and the early stages of the Great Ordovician Biodiversification Event.

The discovery of the Fezouata biota in the latest Tremadocian of southeastern Morocco has significantly changed
our understanding of the early Phanerozoic radiation. The shelly fossil record shows a well-recognized pattern of macroevolutionary
stasis between the Cambrian Explosion and the Great Ordovician Biodiversification Event, but the rich soft-bodied
Fezouata biota paints a different evolutionary picture. The Fezouata assemblage includes a considerable component of
Cambrian holdovers alongside a surprising number of crown group taxa previously unknown to have evolved by the Early
Ordovician. Study of the Fezouata biota is in its early stages, and future discoveries will continue to enrich our view of the
dynamics of the early Phanerozoic radiation and of the nature of the fossil record.

During these last years, considerable attention has been given to unconventional oil and gas shale in northern Africa where the most productive Paleozoic basins are located (e.g. Berkine, Illizi, Kufra, Murzuk, Tindouf, Ahnet, Oued Mya, Mouydir, etc). In most petroleum systems, which characterize these basins, the Silurian played the main role in hydrocarbon generation with two main ‘hot’ shale levels distributed in different locations (basins) and their deposition was restricted to the Rhuddanian (Lllandovery: early Silurian) and the Ludlow-Pridoli (late Silurian). A third major hot shale level had been identified in the Frasnian (Upper Devonian). Southern Tunisia is characterized by three main Paleozoic sedimentary basins, which are from North to South, the southern Chotts, Jeffara and Berkine Basin. They are separated by a major roughly E-W trending lower Paleozoic structural high, which encompass the Mehrez-Oued Hamous uplift to the West (Algeria) and the Nefusa uplift to the East (Libya), passing by the Touggourt-Talemzane-PGA-Bou Namcha (TTPB) structure close to southern Tunisia. The forementioned major source rocks in southern Tunisia are defined by hot shales with elevated Gamma ray values often exceeding 1400 API (in Hayatt-1 well), deposited in deep water environments during short lived (c. 2 Ma) periods of anoxia. In the course of this review, thickness, distribution and maturity maps have been established for each hot shale level using data for more than 70 wells located in both Tunisia and Algeria. Mineralogical modeling was achievd using Spectral Gamma Ray data (U, Th, K), SopectroLith logs (to acquire data for Fe, Si and Ti) and Elemental capture Spectroscopy (ECS). The latter technique provided data for quartz, pyrite, carbonate, clay and Sulfur. In addition to this, the Gamma Ray (GR), Neutron Porosity (ΦN), deep Resistivity (Rt) and Bulk Density (ρb) logs were used to model bulk mineralogy and lithology. Biostratigraphic and complete geochemical review has been undertaken from published papers and unpublished internal reports to better assess these important source intervals.

This map folio should be referenced as:
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.
Also see: 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. https://www.academia.edu/16744278/Atlas_of_Silurian_and_Middle-Late_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 (cscotese@gmail.com). 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.

Phylotectonics is the study of descendant/antecedent relationships between continents, paleocontinents, and terranes based on their plate tectonic history.  This "Tectonic Tree" diagram illustrates the phylotectonic relationships of the major continents, paleocontinents, and terranes during the last 1.5 billion years.  For a description and discussion of how this diagram was created see Scotese (2017) , "Atlas of Oceans  & Continents: Plate Tectonics 1.5 billion years - Today."

Hypogenic speleogenesis is the formation of solution-enlarged permeability structures by waters ascending to a cave-forming zone from below in leaky confined conditions, where deeper groundwaters in regional or intermediate flow systems interact with shallower and more local groundwater flow systems. This is in contrast to more familiar epigenic speleogenesis which is dominated by shallow groundwater systems receiving recharge from the overlying or immediately adjacent surface.Hypogenic caves are identified in various geological and tectonic settings, formed by different dissolutional mechanisms operating in various lithologies. Despite these variations, resultant caves demonstrate a remarkable similarity in patterns and meso-morphology, which strongly suggests that the hydrogeologic settings were broadly identical in their formation. Hypogenic caves commonly demonstrate a characteristic suite of cave morphologies resulting from rising flow across the cave-forming zone with distinct buoyancy-dissolution components. In addition to hydrogeological criteria (hydrostratigraphic position, recharge–discharge configuration and flow pattern viewed from the perspective of the evolution of a regional groundwater flow system), morphogenetic analysis is the primary tool in identifying hypogenic caves.Cave patterns resulting from ascending transverse speleogenesis are strongly guided by the permeability structure in a cave formation. They are also influenced by the discordance of permeability structure in the adjacent beds and by the overall hydrostratigraphic arrangement. Three-dimensional mazes with multiple storeys, or complex 3-D cave systems are most common, although single isolated chambers, passages or crude clusters of a few intersecting passages may occur where fracturing is scarce and laterally discontinuous. Large rising shafts and collapse sinkholes over large voids, associated with deep hydrothermal systems, are also known.Hypogenic caves include many of the largest, by integrated length and by volume, documented caves in the world. More importantly, hypogenic speleogenesis is much more widespread than it was previously presumed. Growing recognition of hypogenic speleogenesis and improved understanding of its peculiar characteristics has an immense importance to both karst science and applied fields as it promises to answer many questions about karst porosity (especially as deep-seated settings are concerned) which remained poorly addressed within the traditional epigenetic karst paradigm.

East and Southeast Asia is a complex assembly of allochthonous continental terranes, island arcs, accretionary complexes
and small ocean basins. The boundaries between continental terranes are marked by major fault zones or by sutures recognized
by the presence of ophiolites, m61anges and accretionary complexes. Stratigraphical, sedimentological,
paleobiogeographical and paleomagnetic data suggest that all of the East and Southeast Asian continental terranes were derived
directly or indirectly from the Iran-Himalaya-Australia margin of Gondwanaland. The evolution of the terranes is one of rifting
from Gondwanaland, northwards drift and amalgamation/accretion to form present day East Asia. Three continental slivers were
rifted from the northeast margin of Gondwanaland in the Silurian-Early Devonian (North China, South China, lndochina/East
Malaya, Qamdo-Simao and Tarim terranes), Early-Middle Permian (Sibumasu, Lhasa and Qiangtang terranes) and Late Jurassic
(West Burma terrane, Woyla terranes). The northwards drift of these terranes was effected by the opening and closing of three sueessive
Tethys oceans, the Paleo-Tethys, Meso-Tethys and Ceno-Tethys. Terrane assembly took place between the Late Paleozoic
and Cenozoic, but the precise timings of amalgamation and accretion are still contentious. Amalgamation of South China and
Indoehina/East Malaya occurred during the Early Carboniferous along the Song Ma Suture to form "Cathaysialand". Cathaysialand,
together with North China, formed a large continental region within the Paleotethys during the Late Carboniferous and Permian.
Paleomagnetic data indicate that this continental region was in equatorial to low northern paleolatitudes which is consistent
with the tropical Cathaysian flora developed on these terranes. The Tarim terrane (together with the Kunlun, Qaidam and Ala Shan
terranes) accreted to Kazakhstan/Siberia in the Permian. This was followed by the suturing of Sibumasu and Qiangtang to Cathaysialand
in the Late Permian-Early Triassic, largely closing the Paleo-Tethys. North and South China were amalgamated in the Late
Triassic-Early Jurassic and finally welded to Laurasia around the same time. The Lhasa terrane accreted to the Sibumasu-Qiangtang
terrane in the Late Jurassic and the Kurosegawa terrane of Japan, interpreted to he derived from Australian Gondwanaland,
accreted to Japanese Eurasia, also in the Late Jurassic. The West Burma and Woyla terranes drifted northwards during the Late
Jurassic and Early Cretaceous as the Ceno-Tethys opened and the Meso-Tethys was destroyed by subduction beneath Eurasia and
were accreted to proto-Southeast Asia in the Early to Late Cretaceous. The Southwest Borneo and Semitau terranes amalgamated
to each other and accreted to lndochina/East Malaya in the Late Cretaceous and the Hainanese terranes probably accreted to South
China sometime in the Cretaceous