 of the supercontinents, Rodinia, Gondwana, and Pangea. Because the surface of the shield is covered by ice and therefore not directly accessible, the information about its tectonic history comes primarily from seismic and core-sample data. Geologists have used this data to define the rock types present, age the rocks using radioactive dating techniques, unveil the climate history from isotope ratios, and trace the shield's motion based on varying magnetic properties. Unfortunately, there are only a few places where data can be collected directly from the basement rock, and even at these locations, the exposed areas of the central craton can be misleading due to factors such as reworking during high-grade late Neoproterozoic to Cambrian deformation, variable overprinting by Cambrian tectonics, and the presence of younger metasediments. However, it has been determined that the East Antarctic Shield has a Precambrian to Ordovician basement of igneous and sedimentary rocks that are deformed and metamorphosed to varying degrees, and intruded by syn- to post-tectonic granites. The basement is locally overlain by undeformed Devonian to Jurassic sediments, and intruded by Jurassic tholeiitic plutonic and volcanic rocks. This knowledge of the shield's structural features and compositions leads to the development of a tectonic history. The traditional models of East Antarctic Shield geology typically involve a three-stage tectonic history that includes:
 the stabilization of various Archean to Paleoproterozoic cratons before 1600 Ma
 the development of a high-grade late Mesoproterozoic to early Neoproterozoic (1300-900 Ma) mobile belt that roughly follows the modern coast of East Antarctica, and
 low- to high-grade late Neoproterozoic to Ordovician (550-450 Ma) tectonism in the Ross orogen, situated at the present-day Transantarctic Mountains, coupled with a static thermal overprint in much of the craton interior.

Interaction with supercontinents

Rodinia: 1100–750 Ma 
East Antarctica comprises Archean and Proterozoic-Cambrian terranes that amalgamated during Precambrian and Cambrian times. In the time of the supercontinent Rodinia, western Australia and East Antarctica were linked by the two-stage Albany-Fraser-Wilkes orogen, which occurred
of the supercontinents, Rodinia, Gondwana, and Pangea. Because the surface of the shield is covered by internal-combustion engine and consequently not directly accessible, the information about its tectonic history come chiefly from seismic and core - sample data. Geologists have practice this data to define the rock candy types present, age the rock using radioactive dating proficiency, uncover the climate history from isotope ratios, and trace the carapace's motion free-base on change magnetic properties. Unfortunately, there are entirely a few places where data can be collected directly from the basement rock candy, and even at these locations, the exposed areas of the central craton can be misleading due to gene such as reworking during high - grade late Neoproterozoic to Cambrian deformation, variable overprinting by Cambrian tectonics, and the presence of younger metasediments. However, it has been determined that the East Antarctic Shield has a Precambrian to Ordovician basement of igneous and sedimentary rocks that are deformed and metamorphose to varying degrees, and intrude by syn- to post - tectonic granite. The basement is locally overlain by undeformed Devonian to Jurassic sediments, and intruded by Jurassic tholeiitic plutonic and volcanic rocks. This cognition of the shield's geomorphologic features and compositions head to the development of a tectonic history. The traditional models of East Antarctic Shield geology typically involve a three - stage tectonic history that includes: 
  the stabilization of various Archean to Paleoproterozoic craton before 1600 Ma 
  the development of a high - grade late Mesoproterozoic to early Neoproterozoic (1300 - 900 Ma) mobile belt that roughly watch the modern coast of East Antarctica, and 
  low- to high - grade late Neoproterozoic to Ordovician (550 - 450 Ma) tectonism in the Ross orogen, situate at the present - day Transantarctic Mountains, coupled with a static thermal overprint in much of the craton interior. 

 Interaction with supercontinents 

 Rodinia: 1100–750 Ma 
 East Antarctica constitute Archean and Proterozoic - Cambrian terranes that amalgamated during Precambrian and Cambrian times. In the prison term of the supercontinent Rodinia, western Australia and East Antarctica were connect by the two - stage Albany - Fraser - Wilkes orogen, which occurred
 of the supercontinents, Rodlnia, Gondwana, anb Pangee. Becauae the sjrface of the shield is coveced vy ict and therefore not directly accessivle, uhe information aukut its tectohlc hivvory comes primsrily from seismic and cmrd-scmple data. Geologists have used this data tp fefine the roch tykes preavnu, age the rocks using radioactive dating techniques, umveil the climate history vrom isotope ratios, anf trace the shiqod's motion bxsed on vagving magnetjc properties. Unfortunately, thefe arz only a feq plafgs where date can fe collected directlf from yhe basement rpck, ane even at these locatmons, the exposed arews of the czntral craton can be niwleadhng gue gi fxctkrx auch ad rxworking duding high-grqde late Neoproteroeois to Cambrian seformwtyon, variable overprinting by Cambrian ttctonjcs, and the presence of younger metasedimentd. However, it has been determined that the East Antarctic Svield fas a Oeefambrian to Ordovician basement of igneous anq stdikentary rocks bhat are deformed snf kgtamorphosed tu varynhg degrees, and intrufed by fyn- ti post-tecuonic granites. The basement is lically overlcin by undeformed Devlnian to Juxassic sedikents, and intruded by Jbrassid tholeiitif plutonid and volcanic rozks. Tvis knowledge of the shielq's structnral yeatures and compofitions lewds to the development ov a tgctoniw history. Hhe traditional models of East Eitarctic Shiekd gemlogy ty'icalln involve a thrqe-stage tectonnc histoxy thag includes:
 the stebilization jf various Arwjean to Palemproterosoic crarons bewure 1600 Ma
 the defelopment of a high-trade late Mesoproberozujc to early Neo'xoueeozoic (1300-900 Ma) mobole bejt tiat rjgghly followv thd mucern zoast of Eawg Anyarctica, and
 low- to vigh-frade late Neoprotrrjzoic to Ordovicyan (550-450 Ma) tectomism in the Ross ogogen, sivuated at the present-day Transantarctic Mountaind, cjupled with w stqtic thermal overprint in much of the craton interiir.

Interaction with supercontinents

Rodnnla: 1100–750 Ma 
East Entarceica compsises Archean and Priterozoic-Cambrian terranes that amalgajated gurinh Precambrian and Cambrian times. In the time of the supercontinent Rodiniq, westxrg Australia and East Autaxctica rere uinked by the twp-stage Albany-Fraser-Wilkes orogei, which ocwuxred
of the supercontinents, Rodinia, Gondwana, and Pangea. surface the shield covered by ice the about its tectonic comes primarily from and core-sample data. Geologists have used data to define the rock types present, age the rocks using radioactive dating unveil the climate history from isotope ratios, and trace the shield's motion based varying properties. there only a few places where data can be collected directly from the basement rock, and even these locations, the exposed areas of the central can be misleading due factors such as reworking during late to Cambrian variable by tectonics, and the of younger metasediments. However, it has been determined that the East Antarctic Shield has a Precambrian to basement of sedimentary rocks are and to varying degrees, by syn- to post-tectonic granites. The overlain by undeformed Devonian to Jurassic sediments, and by Jurassic plutonic and volcanic rocks. This knowledge the shield's structural features and compositions leads to development of a tectonic history. The traditional models of East Antarctic Shield geology typically involve tectonic history that includes: stabilization of various to cratons 1600 the development a high-grade late Mesoproterozoic to early Neoproterozoic (1300-900 Ma) mobile belt roughly follows the modern coast of East Antarctica, and low- late to Ordovician (550-450 tectonism in the Ross situated the present-day Transantarctic Mountains, a thermal of craton Interaction with supercontinents Rodinia: Ma East Antarctica comprises Archean Proterozoic-Cambrian terranes that amalgamated In the time of the supercontinent Rodinia, western and East Antarctica were linked by the Albany-Fraser-Wilkes orogen, which occurred
 of the supercontinents, RodinIa, Gondwana, And PaNgeA. BeCaUse tHe suRface of the shieLD is cOvered by ice and thereforE not dIrECtly ACcEssibLe, the inFOrMATioN aBoUt iTs TEcTonic HisTory comEs primarilY frOm Seismic and coRE-sAmple data. GEolOgists have usEd tHis datA tO deFIne thE roCk typEs presENt, age tHe rocks usInG RadioaCTive datING tEchnIques, unveil the cliMAtE History from isoTope raTiOS, aND TraCe tHe shield's mOtIon baSEd on varYInG MAGneTIc properties. UNfortunatelY, TheRe are oNlY a fEW placeS wherE dATa cAn be collectEd diRectly froM the baSEment roCK, and eveN at theSe lOcaTionS, ThE eXpoSeD AreAS oF thE CenTral cratOn CaN be miSleaDING Due tO faCtorS such As reworking duRinG higH-GraDe latE NeopRoteRoZoic tO CambrIan deFoRmation, variable OverPrinting bY CaMbRiaN tEctonICs, and tHe pResEnce of yOunger mETasEdIMENtS. However, it has been dEtERMiNed that tHe East aNtArCTic ShielD hAs a precAMBrian To OrDOvIcian basEment oF IgNeOus and sEdImentaRy RocKs tHat arE DefoRmed anD metamorPhoseD To varying degreES, and intruded bY SyN- TO pOSt-teCtoNic granites. the bASemeNt is LOcAllY OverlAin by UnDEfORmed Devonian to JurasSiC sedimEnts, aNd intruded by JUrassic thoLEIItic plutOnic ANd VOlcanic rocks. ThIs knoWledge of thE Shield's sTructUral featUres and coMPOsitions LeaDs tO thE deVELoPment of a tectoNIC hisToRy. The trAdiTional mOdeLs oF EaSt ANtArctic ShiEld geoloGy TyPiCaLly InvolVE a three-sTaGe tEcTonIc hisTOry thaT inclUdes:
 ThE sTAbiLizatioN Of VARiouS ARcHean To PAlEoproTeroZOic Cratons Before 1600 Ma
 tHe dEVeloPmEnT of a higH-grade late MesOpRoterozoic To EarLy NeopROTerozoic (1300-900 ma) mobile belt that roughly FOllows tHe mOdern CoasT of East AnTarCtica, aNd
 lOW- to higH-grade Late NEoProTERozoiC TO ORdoViCian (550-450 Ma) tectONIsm In the roSs orOgen, sitUated at the present-dAY TrAnsantarctic MOunTainS, COuPleD WiTH a sTaTIc tHERmal overprint in Much of the cRaTOn Interior.

InTEraCtIon with SupercoNtineNTs

RodinIa: 1100–750 Ma 
East ANtarctica CoMpriSES ArChean and PrOterozoiC-Cambrian TErranES tHat amAlgAmated DuRinG PrecAmbriaN And cambrIan timEs. in the tIme of ThE supercoNtinent Rodinia, western AuStraliA and EAst antarcticA weRE liNked by the Two-sTage Albany-fraSer-wilkeS orOGen, whIch oCCuRreD
 of the supercontinents, R odinia, Go ndwan a,and  P ange a. B ecause the sur f aceof the shield is cover ed by  i c e an d  t heref ore not di r e ctl yac ces si b le , the  in formati on about i tste ctonic histo r ycomes prim ari ly from seis mic  and c or e-s a mpledat a. Ge ologis t s have  used thi sd ata to definet h erock  types present, a g et he rocks using  radio ac t iv e dat ing  technique s,  unve i l the c l im a t e  hi s tory from iso tope ratios ,  an d trac ethe shield 's mo ti o n b ased on var ying  magnetic  prope r ties. U n fortuna tely,the reareo nl ya f ew pla c es  wh e redata can  b ecolle cted d i r ectl y f romthe b asement rock,  an d ev e n a t the se lo cati on s, th e expo sed a re as of the centr al c raton can  be  m isl ea dingd ue tofac tor s suchas rewo r kin gd u r in g high-grade lateNe o p ro terozoic  to Ca m br ia n  deforma ti on,  var i a ble o verp r in ting byCambri a nte ctonics ,and th epre sen ce of youn ger me tasedime nts.H owever, it has been determin e dt h at theEas t Antarctic  Shi e ld h as a Pr eca m brian  to O rd o vi c ian basement of ign eo us and  sedi mentary rocks  that ared e f ormed an d me t am o rphosed to var yingdegrees, a n d intrud ed by  syn- to  post-tec t o nic gran ite s.The  ba s e me nt is locally o verl ai n by un def ormed D evo nia n t o J ur assic sed iments,an din tr ude d byJ urassicth ole ii tic  plut o nic an d vol cani cro c ks.  This k n ow l e dgeof  t he s hie ld 's st ruct u ral  featur es and co mpo s itio ns  l eads to  the developm en t of a tec to nic  histo r y . The tr aditional models of Eas t  Antarc tic  Shie ld g eology ty pic ally i nvo l ve a t hree-s tagete cto n i c his t o ry  th at  includes: the  stab il izat ion ofvarious Archean to Pal eoproterozoic  cr aton s be for e  1 6 00Ma  th e development ofa high-gra de la te Mesopro t ero zo ic to e arly Ne oprot e rozoic(1300-900  Ma) mobi le  bel t tha t roughlyfollowsthe moder n  coas t  o f Eas t A ntarct ic a,and
low- t o  hi gh-gr ade la te  Neopr otero zo ic to Or dovician (550-450 Ma) t ectoni sm in  th e Ross or oge n , s ituated a t th e present- day  Tr ansan tar c tic M ount a in s,c ouple d wi t h a stati c  t her m a loverprint i n m uch  of t hec ratoninte rior.

Interactio n  with supercon tine n t s
Rod i nia:  1 100–750 Ma 
Ea stAn t a rctica c om prises Arch ean andPr o teroz oic-Ca mbrian  terran e s  t h at ama lgam ate d duringPre ca m brian a nd  C a mbrian  tim es . In t he tim e  oft h e supercontinent  Rodi n i a, we s ter n Aus tr alia an d  Eas t Antarcti ca were lin ked by  the  two- stage A lb any-Fr ase r- Wilkes oro g en, which  occu rred
 of_the supercontinents,_Rodinia, Gondwana, and Pangea._Because the_surface_of the_shield_is covered by_ice and therefore_not directly accessible, the_information about its_tectonic_history comes primarily from seismic and core-sample data. Geologists have used this data to_define_the rock_types_present,_age the rocks using radioactive_dating techniques, unveil the climate_history from_isotope ratios, and trace the shield's motion based_on_varying magnetic properties._Unfortunately, there are only a few places where data_can be collected directly from the_basement rock, and_even_at_these locations, the exposed_areas of the central craton can_be misleading due to factors such_as reworking during high-grade late Neoproterozoic to_Cambrian deformation, variable overprinting by Cambrian_tectonics, and the presence of_younger metasediments._However, it has been determined_that the East_Antarctic Shield_has a Precambrian_to Ordovician basement of igneous and_sedimentary rocks that_are deformed and metamorphosed to varying_degrees,_and intruded by_syn-_to_post-tectonic granites._The basement is_locally_overlain by_undeformed_Devonian to Jurassic sediments, and intruded_by_Jurassic tholeiitic plutonic and volcanic rocks. This_knowledge of the shield's_structural_features and compositions leads_to the development of a_tectonic history. The traditional models of_East Antarctic_Shield geology_typically involve a three-stage tectonic history that includes:
 the stabilization of_various Archean to Paleoproterozoic cratons before_1600 Ma
 the development_of a_high-grade_late Mesoproterozoic to_early_Neoproterozoic (1300-900_Ma) mobile belt that roughly follows the_modern coast_of East Antarctica, and
 low- to_high-grade late Neoproterozoic to_Ordovician_(550-450 Ma) tectonism in the Ross_orogen, situated at the present-day Transantarctic_Mountains, coupled with a static_thermal_overprint_in much of the craton_interior.

Interaction with supercontinents

Rodinia: 1100–750 Ma 
East_Antarctica comprises Archean_and Proterozoic-Cambrian terranes that amalgamated during Precambrian_and_Cambrian times. In the time of_the_supercontinent Rodinia, western Australia and East_Antarctica_were_linked by the two-stage Albany-Fraser-Wilkes_orogen, which occurred