22:
512:
851:
691:
164:
267:
2668:
374:. Similar folds tend to display thinning of the limbs and thickening of the hinge zone. Concentric folds are caused by warping from active buckling of the layers, whereas similar folds usually form by some form of shear flow where the layers are not mechanically active. Ramsay has proposed a classification scheme for folds that often is used to describe folds in profile based upon the curvature of the inner and outer lines of a fold and the behavior of
768:
972:
millions of years, this process is capable of gathering large quantities of trace minerals from large expanses of rock and depositing them at very concentrated sites. This may be a mechanism that is responsible for the veins. To summarize, when searching for veins of valuable minerals, it might be wise to look for highly folded rock, and this is the reason why the mining industry is very interested in the theory of geological folding.
650:
299:
214:
496:
355:
130:
138:
683:
964:
504:
675:
665:
When a sequence of layered rocks is shortened parallel to its layering, this deformation may be accommodated in a number of ways, homogeneous shortening, reverse faulting or folding. The response depends on the thickness of the mechanical layering and the contrast in properties between the layers. If
862:: a competent layer or bed of rock can withstand an applied load without collapsing and is relatively strong, while an incompetent layer is relatively weak. When rock behaves as a fluid, as in the case of very weak rock such as rock salt, or any rock that is buried deeply enough, it typically shows
670:
layers in a less competent matrix control the folding and typically generate classic rounded buckle folds accommodated by deformation in the matrix. In the case of regular alternations of layers of contrasting properties, such as sandstone-shale sequences, kink-bands, box-folds and chevron folds are
257:
Minor folds are quite frequently seen in outcrop; major folds seldom are except in the more arid countries. Minor folds can, however, often provide the key to the major folds they are related to. They reflect the same shape and style, the direction in which the closures of the major folds lie, and
971:
Layers of rock that fold into a hinge need to accommodate large deformations in the hinge zone. This results in voids between the layers. These voids, and especially the fact that the water pressure is lower in the voids than outside of them, act as triggers for the deposition of minerals. Over
711:
Fault-bend folds are caused by displacement along a non-planar fault. In non-vertical faults, the hanging-wall deforms to accommodate the mismatch across the fault as displacement progresses. Fault bend folds occur in both extensional and thrust faulting. In extension, listric faults form
949:
The rheology of the layers being folded determines characteristic features of the folds that are measured in the field. Rocks that deform more easily form many short-wavelength, high-amplitude folds. Rocks that do not deform as easily form long-wavelength, low-amplitude folds.
890:
Flexural slip allows folding by creating layer-parallel slip between the layers of the folded strata, which, altogether, result in deformation. A good analogy is bending a phone book, where volume preservation is accommodated by slip between the pages of the book.
870:, because little resistance is offered): the strata appear shifted undistorted, assuming any shape impressed upon them by surrounding more rigid rocks. The strata simply serve as markers of the folding. Such folding is also a feature of many igneous intrusions and
815:
form in poorly consolidated sediments, they commonly undergo folding, particularly at their leading edges, during their emplacement. The asymmetry of the slump folds can be used to determine paleoslope directions in sequences of sedimentary rocks.
1496:
Reicherter, K.; Froitzheim, N.; Jarosinki, M.; Badura, J.; Franzke, H.-J.; Hansen, M.; HĂĽbscher, C.; MĂĽller, R.; Poprawa, P.; Reinecker, J.; Stackebrandt, W.; Voigt, T.; von
Eynatten, H.; Zuchiewicz, W. (2008).
854:
Flow folding: depiction of the effect of an advancing ramp of rigid rock into compliant layers. Top: low drag by a ramp: layers are not altered in thickness; Bottom: high drag: lowest layers tend to crumple.
922:, a form of metamorphic process, in which rocks shorten by dissolving constituents in areas of high strain and redepositing them in areas of lower strain. Folds generated in this way include examples in
240:. A fold axis “is the closest approximation to a straight line that when moved parallel to itself, generates the form of the fold.” (Ramsay 1967). A fold that can be generated by a fold axis is called a
310:
of each limb), called the interlimb angle. Gentle folds have an interlimb angle of between 180° and 120°, open folds range from 120° to 70°, close folds from 70° to 30°, and tight folds from 30° to 0°.
25:
Folds of alternate layers of limestone and chert occur in Greece. The limestone and chert were originally deposited as flat layers on the floor of a deep sea basin. These folds were produced by
984:, oil accumulating in the crest of the fold. Most anticlinal traps are produced as a result of sideways pressure, folding the layers of rock, but can also occur from sediments being compacted.
732:
are caused when displacement occurs on an existing fault without further propagation. In both reverse and normal faults this leads to folding of the overlying sequence, often in the form of a
790:
typically contain minor asymmetric folds, with the direction of overturning consistent with the overall shear sense. Some of these folds have highly curved hinge-lines and are referred to as
918:
If the folding deformation cannot be accommodated by a flexural slip or volume-change shortening (buckling), the rocks are generally removed from the path of the stress. This is achieved by
838:. In the case of high-level intrusions, near the Earth's surface, this deformation is concentrated above the intrusion and often takes the form of folding, as with the upper surface of a
190:
portions; the limbs are the flanks of the fold, and the limbs converge at the hinge zone. Within the hinge zone lies the hinge point, which is the point of minimum radius of
804:
Recently deposited sediments are normally mechanically weak and prone to remobilization before they become lithified, leading to folding. To distinguish them from folds of
980:
Anticlinal traps are formed by folding of rock. For example, if a porous sandstone unit covered with low permeability shale is folded into an anticline, it may form a
1585:
1336:
703:
Many folds are directly related to faults, associated with their propagation, displacement and the accommodation of strains between neighboring faults.
910:. Folding under this mechanism is typical of a similar fold style, as thinned limbs are shortened horizontally and thickened hinges do so vertically.
796:. Folds in shear zones can be inherited, formed due to the orientation of pre-shearing layering or formed due to instability within the shear flow.
56:. Folds in rocks vary in size from microscopic crinkles to mountain-sized folds. They occur as single isolated folds or in periodic sets (known as
720:
form whenever a thrust fault cuts up section from one detachment level to another. Displacement over this higher-angle ramp generates the folding.
1370:
902:
Typically, folding is thought to occur by simple buckling of a planar surface and its confining volume. The volume change is accommodated by
792:
2005:
882:
Folding of rocks must balance the deformation of layers with the conservation of volume in a rock mass. This occurs by several mechanisms.
1440:
614:
Parasitic: short-wavelength folds formed within a larger wavelength fold structure - normally associated with differences in bed thickness
1650:
1534:
822:
Compaction: Folds can be generated in a younger sequence by differential compaction over older structures such as fault blocks and
306:
Fold tightness is defined by the size of the angle between the fold's limbs (as measured tangential to the folded surface at the
225:
is defined as a plane connecting all the hinge lines of stacked folded surfaces. If the axial surface is planar, it is called an
99:. Folds are commonly formed by shortening of existing layers, but may also be formed as a result of displacement on a non-planar
1498:
1696:
1662:
1510:
1416:
1382:
1346:
1319:
1193:
175:
is the line joining points of maximum curvature on a folded surface. This line may be either straight or curved. The term
2248:
1686:
604:
Slump: typically monoclinal, the result of differential compaction or dissolution during sedimentation and lithification.
1624:
819:
Dewatering: Rapid dewatering of sandy sediments, possibly triggered by seismic activity, can cause convolute bedding.
1720:
327:
Not all folds are equal on both sides of the axis of the fold. Those with limbs of relatively equal length are termed
244:. This term has been broadened to include near-cylindrical folds. Often, the fold axis is the same as the hinge line.
1950:
1927:
1810:
1788:
1761:
1289:
1255:
1226:
1168:
1139:
1076:
21:
2702:
1998:
1309:
566:
Recumbent: linear, fold axial plane oriented at a low angle resulting in overturned strata in one limb of the fold.
258:
their cleavage indicates the attitude of the axial planes of the major folds and their direction of overturning
1721:"Productive Large Scale Folding Associated with Igneous Intrusions: El Trapial Field, Neuquen Basin, Argentina"
2697:
2033:
1406:
1106:
2692:
2671:
1991:
335:. Asymmetrical folds generally have an axis at an angle to the original unfolded surface they formed on.
744:
When a thrust fault continues to displace above a planar detachment without further fault propagation,
666:
the layering does begin to fold, the fold style is also dependent on these properties. Isolated thick
2333:
53:
748:
may form, typically of box-fold style. These generally occur above a good detachment such as in the
2338:
2114:
2602:
1826:
Hudleston, P. J. (1977). "Similar folds, recumbent folds and gravity tectonics in ice and rocks".
2104:
2038:
1754:
Folding of viscous layers: mechanical analysis and interpretation of structures in deformed rock
1471:
835:
654:
1798:
1778:
1243:
1218:
1129:
511:
2615:
2419:
2308:
2178:
2158:
2058:
2028:
1749:
1273:
1156:
607:
Ptygmatic: Folds are chaotic, random and disconnected. Typical of sedimentary slump folding,
1978:
1919:
1910:
1891:
1562:
1210:
2592:
2476:
2193:
2148:
1973:
1877:
1835:
1600:
1546:
1455:
1094:
946:, or method of response to stress, of the rock at the time at which the stress is applied.
667:
112:
76:
8:
2625:
2501:
2486:
2463:
2459:
2238:
2163:
2063:
2048:
713:
152:
1839:
1604:
1550:
1459:
1098:
61:
2574:
2471:
2353:
2258:
2173:
2138:
2068:
2014:
1859:
1851:
1616:
927:
850:
359:
343:
34:
1045:
2610:
2544:
2496:
2491:
2371:
2361:
2303:
2078:
1946:
1923:
1863:
1806:
1784:
1757:
1692:
1658:
1620:
1506:
1412:
1378:
1342:
1315:
1285:
1251:
1222:
1211:
1189:
1164:
1135:
1110:
1072:
1049:
1003:
993:
919:
690:
596:
275:
148:
84:
1377:. Vol. Special Publications 253. Geological Society, London. pp. 285–305.
894:
The fold formed by the compression of competent rock beds is called "flexure fold".
625:
involves strata dipping in the same direction, though not necessarily any folding.)
319:, have an interlimb angle of between 10° and zero, with essentially parallel limbs.
2414:
2409:
2343:
2318:
2313:
2288:
2228:
2188:
2043:
1843:
1608:
1554:
1463:
1102:
1041:
586:
516:
307:
203:
199:
80:
68:
42:
1939:
182:
A fold surface seen perpendicular to its shortening direction can be divided into
2653:
2549:
2449:
2424:
2396:
2381:
2283:
2233:
2223:
2218:
2094:
812:
808:
origin, such structures are called synsedimentary (formed during sedimentation).
745:
638:
195:
100:
1184:
Barnes, J. W.; Lisle, Richard J. (2013). "5 Field
Measurements and Techniques".
2554:
2516:
2386:
2366:
2278:
2203:
2198:
2153:
2119:
2109:
2053:
1008:
981:
749:
576:
230:
26:
2168:
1688:
Nontechnical guide to petroleum geology, exploration, drilling, and production
1558:
1467:
2686:
2444:
1114:
1053:
563:: linear, strata dip in one direction between horizontal layers on each side.
378:. that is, lines connecting points of equal dip on adjacent folded surfaces:
141:
88:
72:
1408:
Structural analysis and synthesis: a laboratory course in structural geology
2439:
2099:
2073:
1128:
Ghosh, Subir Kumar; Naha, Kshitindramohan (1997). Sengupta, Sudipta (ed.).
1013:
939:
787:
780:
617:
Disharmonic: Folds in adjacent layers with different wavelengths and shapes
332:
551:: linear, strata dip away from the axial center, age unknown, or inverted.
207:
2620:
2506:
2481:
2434:
2429:
2404:
2293:
2213:
2183:
1244:"Figure 10.14: Classification of fold profiles using dip isogon patterns"
658:
266:
198:
of the fold represents the highest point of the fold surface whereas the
1855:
1441:"Style and sequence of deformation during extensional fault-propagation"
495:
354:
163:
2648:
2635:
2143:
834:
The emplacement of igneous intrusions tends to deform the surrounding
776:
557:: linear, strata dip toward the axial center, age unknown, or inverted.
287:
2253:
963:
767:
2584:
2564:
2559:
2539:
2521:
2511:
2323:
2268:
2130:
1983:
923:
839:
756:
733:
634:
622:
608:
560:
528:
191:
123:
119:
1586:"Paleoslope Analysis of Slump Folds in the Devonian Flysch of Maine"
2643:
2569:
1847:
1612:
1495:
1371:"Geometric and experimental models of extensional fault-bend folds"
943:
805:
772:
753:
649:
548:
538:
328:
298:
144:
213:
2376:
2328:
2273:
1405:
Rowland, S. M.; Duebendorfer, E. M.; Schieflebein, I. M. (2007).
998:
871:
554:
129:
116:
96:
45:
682:
137:
2243:
2208:
1404:
283:
91:. A set of folds distributed on a regional scale constitutes a
210:
reverses; on regular folds, this is the midpoint of the limb.
2263:
1963:: McGraw-Hill Book Company, New York, 560pp., ISBN 193066589X
346:
is calculated in a direction perpendicular to the fold axis.
1131:
Evolution of geological structures in micro- to macro-scales
579:: nonlinear, strata dip away from center in all directions,
503:
2298:
1375:
Analogue and numerical modelling of crustal-scale processes
823:
674:
366:
Folds that maintain uniform layer thickness are classed as
1439:
Jackson, C. A. L.; Gawthorpe, R. L.; Sharp, I. R. (2006).
1274:"Figure 3.12: Fold classification based upon dip diagrams"
1085:
Donath, F. A.; Parker, R. B. (1964). "Folds and
Folding".
531:: linear, strata normally dip away from the axial center,
1341:. Vol. 2 (3 ed.). Academic Press. p. 392.
589:: nonlinear, strata dip toward center in all directions,
1067:
Davis, George H.; Reynolds, Stephen J. (1996). "Folds".
1651:"17. Sediments into rocks: post-depositional processes"
541:: linear, strata normally dip toward the axial center,
64:
folds are those formed during sedimentary deposition.
1532:
1438:
1107:
10.1130/0016-7606(1964)75[45:FAF]2.0.CO;2
1071:. New York: John Wiley & Sons. pp. 372–424.
444:
Orthogonal thickness at limbs narrower than at hinge
424:
Orthogonal thickness at hinge narrower than at limbs
599:: angular fold with straight limbs and small hinges
278:, with planar limbs meeting at an angular axis, as
1938:
1918:. Upper Saddle River, NJ: Prentice Hall. pp.
1909:
1718:
1505:. Geological Society, London. pp. 1233–1285.
1032:Fleury, M. J. (1964). "The description of folds".
286:with a curved axis, or as elliptical with unequal
41:is a stack of originally planar surfaces, such as
1878:"Geological Folding and the Presence of Minerals"
1368:
133:Kink band folds in the Permian of New Mexico, USA
2684:
1937:Pollard, David D.; Fletcher, Raymond C. (2005).
1748:Johnson, Arvid M.; Fletcher, Raymond C. (1994).
1303:
1301:
858:The compliance of rock layers is referred to as
1936:
1747:
1719:Orchuela, I.; Lara, M. E.; Suarez, M. (2003).
1533:Carreras, J.; Druguet, E.; Griera, A. (2005).
206:of a fold is the point on a limb at which the
87:, and even as primary flow structures in some
1999:
1805:(2nd ed.). Macmillan. pp. 241–242.
1583:
1298:
1242:Price, Neville J.; Cosgrove, John W. (1990).
1241:
1066:
545:strata in center irrespective of orientation.
535:strata in center irrespective of orientation.
1916:Physical Geography: A Landscape Appreciation
1907:
1411:(3 ed.). Wiley-Blackwell. p. 301.
1373:. In Buiter, S. J. H.; Schreurs, G. (eds.).
1084:
723:
644:
349:
1796:
1338:The techniques of modern structural geology
1334:
1264:
1250:. Cambridge University Press. p. 246.
1213:Geological Structures and Maps: 3rd Edition
1183:
2006:
1992:
1369:Withjack, M. O.; Schlische, R. W. (2006).
1034:Proceedings of the Geologists' Association
331:, and those with highly unequal limbs are
1825:
1756:. Columbia University Press. p. 87.
1127:
762:
507:A monocline at Colorado National Monument
79:, as evidenced by their presence in soft
1783:(3rd ed.). Routledge. p. 109.
1499:"19. Alpine Tectonics north of the Alps"
1362:
962:
953:
849:
766:
752:, where the detachment occurs on middle
698:
689:
681:
673:
648:
510:
502:
494:
353:
297:
265:
212:
162:
136:
128:
20:
1908:McKnight, Tom L.; Hess, Darrel (2000).
1741:
1648:
1577:
1398:
1163:(3rd ed.). Routledge. p. 26.
1069:Structural Geology of Rocks and Regions
942:in which the rocks are located and the
938:Folds in the rock are formed about the
933:
799:
641:. They arise from a variety of causes.
382:Ramsay classification scheme for folds
247:
2685:
2013:
1892:"Oil and gas traps - Energy Education"
1770:
1489:
1328:
1280:(3rd ed.). Routledge. p. 31
1087:Geological Society of America Bulletin
1031:
716:in their hanging walls. In thrusting,
338:
115:or due to the effects of a high-level
107:), at the tip of a propagating fault (
67:Folds form under varied conditions of
1987:
1526:
1314:(3 ed.). Routledge. p. 33.
1209:Lisle, Richard J. (2004). "Folding".
1208:
1188:. John Wiley & Sons. p. 79.
1186:Basic geological mapping: 4th Edition
926:and areas with a strong axial planar
877:
739:
706:
194:(maximum curvature) of the fold. The
179:has also been used for this feature.
1819:
1799:"Figure 12.8: Passive shear folding"
1797:Twiss, R. J.; Moores, E. M. (1992).
1776:
1684:
1678:
1642:
1335:Ramsay, J. G.; Huber, M. I. (1987).
1307:
1271:
1235:
1154:
913:
829:
628:
370:folds. Those that do not are called
2249:List of tectonic plate interactions
1148:
1121:
633:Folds appear on all scales, in all
158:
16:Stack of originally planar surfaces
13:
1941:Fundamentals of Structural Geology
1901:
958:
358:Ramsay classification of folds by
14:
2714:
1967:
1911:"The Internal Processes: Folding"
1780:Foundations of structural geology
1278:Foundations of structural geology
1248:Analysis of geological structures
1161:Foundations of structural geology
611:and decollement detachment zones.
293:
229:and can be described in terms of
2667:
2666:
1657:. Wiley-Blackwell. p. 355.
1584:Bradley, D.; Hanson, L. (1998).
1311:Foundation of Structural Geology
885:
786:Shear zones that approximate to
490:
322:
1961:Folding and fracturing of rocks
1955:– via Archive Foundation.
1932:– via Archive Foundation.
1884:
1870:
1712:
1691:. PennWell Books. p. 598.
1432:
975:
845:
380:
1945:. Cambridge University Press.
1655:Sedimentology and stratigraphy
1202:
1177:
1060:
1025:
1:
1539:Journal of Structural Geology
1503:The Geology of Central Europe
1448:Journal of Structural Geology
1046:10.1016/S0016-7878(64)80023-7
771:Dextral sense shear folds in
261:
483:
473:
470:
461:
451:
448:
443:
441:
438:
433:
431:
428:
423:
421:
418:
413:
403:
400:
395:
389:
362:of dip isogons (red lines).
274:A fold can be shaped like a
252:
7:
1157:"Fold axis and axial plane"
987:
906:the volume, which grows in
897:
728:Fault propagation folds or
48:, that are bent or curved (
10:
2719:
1535:"Shear zone-related folds"
499:An anticline in New Jersey
462:Dip isogons are parallel:
2662:
2634:
2601:
2583:
2530:
2458:
2395:
2352:
2334:Thick-skinned deformation
2128:
2087:
2021:
1559:10.1016/j.jsg.2004.08.004
1468:10.1016/j.jsg.2005.11.009
1134:. Springer. p. 222.
904:layer parallel shortening
724:Fault propagation folding
645:Layer-parallel shortening
522:
439: 1C
429: 1B
419: 1A
350:Deformation style classes
202:is the lowest point. The
2339:Thin-skinned deformation
2115:Stereographic projection
1019:
570:
2703:Deformation (mechanics)
2105:Orthographic projection
2088:Measurement conventions
2034:Lamé's stress ellipsoid
1501:. In McCann, T. (ed.).
637:, at all levels in the
83:, the full spectrum of
968:
855:
783:
763:Folding in shear zones
695:
694:Fault-propagation fold
687:
679:
662:
655:La Herradura Formation
519:
508:
500:
363:
303:
282:with curved limbs, as
271:
270:Chevron folds, Ireland
218:
168:
155:
134:
109:fault propagation fold
95:, a common feature of
30:
2616:Paleostress inversion
2309:Strike-slip tectonics
2179:Extensional tectonics
2159:Continental collision
2029:Deformation mechanism
1217:. Elsevier. pp.
966:
954:Economic implications
853:
770:
699:Fault-related folding
693:
685:
677:
652:
514:
506:
498:
414:Dip isogons converge
357:
301:
269:
216:
166:
140:
132:
24:
2698:Geological processes
2194:Fold and thrust belt
1959:Ramsay, J.G., 1967,
1777:Park, R. G. (1997).
1685:Hyne, N. J. (2001).
1649:Nichols, G. (1999).
1308:Park, R. G. (2004).
1272:Park, R. G. (2004).
1155:Park, R. G. (2004).
934:Mechanics of folding
920:pressure dissolution
811:Slump folding: When
800:Folding in sediments
484:Dip isogons diverge
248:Descriptive features
167:Fold sketch 3D model
77:temperature gradient
2626:Section restoration
2502:Rock microstructure
2164:Convergent boundary
2064:Strain partitioning
2049:Overburden pressure
2039:Mohr–Coulomb theory
1840:1977JG.....85..113H
1605:1998JG....106..305B
1551:2005JSG....27.1229C
1460:2006JSG....28..519J
1099:1964GSAB...75...45D
714:rollover anticlines
671:normally produced.
383:
339:Facing and vergence
153:Barstow, California
111:), by differential
52:) during permanent
2693:Structural geology
2603:Kinematic analysis
2259:Mountain formation
2174:Divergent boundary
2139:Accretionary wedge
2015:Structural geology
1828:Journal of Geology
1803:Structural geology
1593:Journal of Geology
1270:See, for example,
969:
967:anticline oil trap
878:Folding mechanisms
856:
784:
740:Detachment folding
707:Fault bend folding
696:
688:
680:
678:Rollover anticline
663:
520:
509:
501:
381:
364:
304:
272:
219:
169:
156:
135:
35:structural geology
31:
27:Alpine deformation
2680:
2679:
2611:3D fold evolution
2497:Pressure solution
2492:Oblique foliation
2372:Exfoliation joint
2362:Columnar jointing
2022:Underlying theory
1979:Oil and gas traps
1698:978-0-87814-823-3
1664:978-0-632-03578-6
1565:on 17 August 2012
1512:978-1-86239-264-9
1418:978-1-4051-1652-7
1384:978-1-86239-191-8
1348:978-0-12-576922-8
1321:978-0-7487-5802-9
1195:978-1-118-68542-6
1004:Mountain building
994:3D fold evolution
982:hydrocarbons trap
914:Mass displacement
830:Igneous intrusion
629:Causes of folding
593:strata in center.
583:strata in center.
488:
487:
236:Folds can have a
217:Flank & hinge
149:Barstow Formation
85:metamorphic rocks
2710:
2670:
2669:
2415:Detachment fault
2410:Cataclastic rock
2344:Thrust tectonics
2314:Structural basin
2289:Pull-apart basin
2229:Horst and graben
2008:
2001:
1994:
1985:
1984:
1956:
1944:
1933:
1913:
1896:
1895:
1888:
1882:
1881:
1874:
1868:
1867:
1823:
1817:
1816:
1794:
1774:
1768:
1767:
1745:
1739:
1738:
1736:
1734:
1725:
1716:
1710:
1709:
1707:
1705:
1682:
1676:
1675:
1673:
1671:
1646:
1640:
1639:
1637:
1635:
1629:
1623:. Archived from
1590:
1581:
1575:
1574:
1572:
1570:
1561:. Archived from
1545:(7): 1229–1251.
1530:
1524:
1523:
1521:
1519:
1493:
1487:
1486:
1484:
1482:
1476:
1470:. Archived from
1445:
1436:
1430:
1429:
1427:
1425:
1402:
1396:
1395:
1393:
1391:
1366:
1360:
1359:
1357:
1355:
1332:
1326:
1325:
1305:
1296:
1295:
1268:
1262:
1261:
1239:
1233:
1232:
1216:
1206:
1200:
1199:
1181:
1175:
1174:
1152:
1146:
1145:
1125:
1119:
1118:
1082:
1064:
1058:
1057:
1029:
746:detachment folds
517:King Oscar Fjord
515:Recumbent fold,
384:
302:Interlimb angles
242:cylindrical fold
204:inflection point
159:Fold terminology
2718:
2717:
2713:
2712:
2711:
2709:
2708:
2707:
2683:
2682:
2681:
2676:
2658:
2630:
2597:
2579:
2550:Detachment fold
2526:
2454:
2450:Transform fault
2425:Fault mechanics
2391:
2348:
2284:Plate tectonics
2234:Intra-arc basin
2124:
2095:Brunton compass
2083:
2017:
2012:
1970:
1953:
1930:
1904:
1902:Further reading
1899:
1890:
1889:
1885:
1876:
1875:
1871:
1824:
1820:
1813:
1791:
1775:
1771:
1764:
1746:
1742:
1732:
1730:
1723:
1717:
1713:
1703:
1701:
1699:
1683:
1679:
1669:
1667:
1665:
1647:
1643:
1633:
1631:
1630:on 17 July 2011
1627:
1588:
1582:
1578:
1568:
1566:
1531:
1527:
1517:
1515:
1513:
1494:
1490:
1480:
1478:
1477:on 16 June 2011
1474:
1443:
1437:
1433:
1423:
1421:
1419:
1403:
1399:
1389:
1387:
1385:
1367:
1363:
1353:
1351:
1349:
1333:
1329:
1322:
1306:
1299:
1292:
1269:
1265:
1258:
1240:
1236:
1229:
1207:
1203:
1196:
1182:
1178:
1171:
1153:
1149:
1142:
1126:
1122:
1079:
1065:
1061:
1030:
1026:
1022:
990:
978:
961:
959:Mining industry
956:
936:
916:
900:
888:
880:
868:passive folding
848:
832:
802:
765:
742:
726:
718:ramp anticlines
709:
701:
647:
631:
573:
525:
493:
481:
477:
459:
455:
434:Parallel folds
411:
407:
352:
341:
325:
317:isoclinal folds
308:inflection line
296:
264:
255:
250:
161:
105:fault bend fold
17:
12:
11:
5:
2716:
2706:
2705:
2700:
2695:
2678:
2677:
2675:
2674:
2663:
2660:
2659:
2657:
2656:
2651:
2646:
2640:
2638:
2632:
2631:
2629:
2628:
2623:
2618:
2613:
2607:
2605:
2599:
2598:
2596:
2595:
2589:
2587:
2581:
2580:
2578:
2577:
2572:
2567:
2562:
2557:
2552:
2547:
2542:
2536:
2534:
2528:
2527:
2525:
2524:
2519:
2517:Tectonic phase
2514:
2509:
2504:
2499:
2494:
2489:
2484:
2479:
2474:
2468:
2466:
2456:
2455:
2453:
2452:
2447:
2442:
2437:
2432:
2427:
2422:
2417:
2412:
2407:
2401:
2399:
2393:
2392:
2390:
2389:
2384:
2379:
2374:
2369:
2364:
2358:
2356:
2350:
2349:
2347:
2346:
2341:
2336:
2331:
2326:
2321:
2316:
2311:
2306:
2301:
2296:
2291:
2286:
2281:
2279:Passive margin
2276:
2271:
2266:
2261:
2256:
2251:
2246:
2241:
2236:
2231:
2226:
2221:
2216:
2211:
2206:
2204:Foreland basin
2201:
2199:Fold mountains
2196:
2191:
2186:
2181:
2176:
2171:
2166:
2161:
2156:
2154:Back-arc basin
2151:
2146:
2141:
2135:
2133:
2126:
2125:
2123:
2122:
2120:Strike and dip
2117:
2112:
2107:
2102:
2097:
2091:
2089:
2085:
2084:
2082:
2081:
2076:
2071:
2066:
2061:
2056:
2054:Rock mechanics
2051:
2046:
2041:
2036:
2031:
2025:
2023:
2019:
2018:
2011:
2010:
2003:
1996:
1988:
1982:
1981:
1976:
1969:
1968:External links
1966:
1965:
1964:
1957:
1951:
1934:
1928:
1903:
1900:
1898:
1897:
1883:
1869:
1848:10.1086/628272
1834:(1): 113–122.
1818:
1811:
1789:
1769:
1762:
1740:
1728:AAPG Abstracts
1711:
1697:
1677:
1663:
1641:
1613:10.1086/516024
1599:(3): 305–318.
1576:
1525:
1511:
1488:
1454:(3): 519–535.
1431:
1417:
1397:
1383:
1361:
1347:
1327:
1320:
1297:
1290:
1263:
1256:
1234:
1227:
1201:
1194:
1176:
1169:
1147:
1140:
1120:
1077:
1059:
1040:(4): 461–492.
1023:
1021:
1018:
1017:
1016:
1011:
1009:Rock mechanics
1006:
1001:
996:
989:
986:
977:
974:
960:
957:
955:
952:
935:
932:
915:
912:
899:
896:
887:
884:
879:
876:
847:
844:
831:
828:
801:
798:
764:
761:
750:Jura Mountains
741:
738:
730:tip-line folds
725:
722:
708:
705:
700:
697:
686:Ramp anticline
646:
643:
630:
627:
619:
618:
615:
612:
605:
602:
600:
594:
584:
572:
569:
568:
567:
564:
558:
552:
546:
536:
524:
521:
492:
489:
486:
485:
482:
479:
475:
472:
468:
467:
460:
457:
453:
450:
446:
445:
442:
440:
436:
435:
432:
430:
426:
425:
422:
420:
416:
415:
412:
409:
405:
402:
398:
397:
394:
388:
351:
348:
340:
337:
324:
321:
295:
294:Fold tightness
292:
263:
260:
254:
251:
249:
246:
231:strike and dip
160:
157:
97:orogenic zones
62:Synsedimentary
15:
9:
6:
4:
3:
2:
2715:
2704:
2701:
2699:
2696:
2694:
2691:
2690:
2688:
2673:
2665:
2664:
2661:
2655:
2652:
2650:
2647:
2645:
2642:
2641:
2639:
2637:
2633:
2627:
2624:
2622:
2619:
2617:
2614:
2612:
2609:
2608:
2606:
2604:
2600:
2594:
2591:
2590:
2588:
2586:
2582:
2576:
2573:
2571:
2568:
2566:
2563:
2561:
2558:
2556:
2553:
2551:
2548:
2546:
2543:
2541:
2538:
2537:
2535:
2533:
2529:
2523:
2520:
2518:
2515:
2513:
2510:
2508:
2505:
2503:
2500:
2498:
2495:
2493:
2490:
2488:
2485:
2483:
2480:
2478:
2475:
2473:
2470:
2469:
2467:
2465:
2461:
2457:
2451:
2448:
2446:
2445:Transfer zone
2443:
2441:
2438:
2436:
2433:
2431:
2428:
2426:
2423:
2421:
2418:
2416:
2413:
2411:
2408:
2406:
2403:
2402:
2400:
2398:
2394:
2388:
2385:
2383:
2380:
2378:
2375:
2373:
2370:
2368:
2365:
2363:
2360:
2359:
2357:
2355:
2351:
2345:
2342:
2340:
2337:
2335:
2332:
2330:
2327:
2325:
2322:
2320:
2317:
2315:
2312:
2310:
2307:
2305:
2302:
2300:
2297:
2295:
2292:
2290:
2287:
2285:
2282:
2280:
2277:
2275:
2272:
2270:
2267:
2265:
2262:
2260:
2257:
2255:
2252:
2250:
2247:
2245:
2242:
2240:
2237:
2235:
2232:
2230:
2227:
2225:
2222:
2220:
2217:
2215:
2212:
2210:
2207:
2205:
2202:
2200:
2197:
2195:
2192:
2190:
2187:
2185:
2182:
2180:
2177:
2175:
2172:
2170:
2167:
2165:
2162:
2160:
2157:
2155:
2152:
2150:
2147:
2145:
2142:
2140:
2137:
2136:
2134:
2132:
2127:
2121:
2118:
2116:
2113:
2111:
2108:
2106:
2103:
2101:
2098:
2096:
2093:
2092:
2090:
2086:
2080:
2077:
2075:
2072:
2070:
2067:
2065:
2062:
2060:
2057:
2055:
2052:
2050:
2047:
2045:
2044:Mohr's circle
2042:
2040:
2037:
2035:
2032:
2030:
2027:
2026:
2024:
2020:
2016:
2009:
2004:
2002:
1997:
1995:
1990:
1989:
1986:
1980:
1977:
1975:
1974:Mark Peletier
1972:
1971:
1962:
1958:
1954:
1952:0-521-83927-0
1948:
1943:
1942:
1935:
1931:
1929:0-13-020263-0
1925:
1921:
1917:
1912:
1906:
1905:
1893:
1887:
1879:
1873:
1865:
1861:
1857:
1853:
1849:
1845:
1841:
1837:
1833:
1829:
1822:
1814:
1812:0-7167-2252-6
1808:
1804:
1800:
1792:
1790:0-7487-5802-X
1786:
1782:
1781:
1773:
1765:
1763:0-231-08484-6
1759:
1755:
1751:
1744:
1729:
1722:
1715:
1700:
1694:
1690:
1689:
1681:
1666:
1660:
1656:
1652:
1645:
1626:
1622:
1618:
1614:
1610:
1606:
1602:
1598:
1594:
1587:
1580:
1564:
1560:
1556:
1552:
1548:
1544:
1540:
1536:
1529:
1514:
1508:
1504:
1500:
1492:
1473:
1469:
1465:
1461:
1457:
1453:
1449:
1442:
1435:
1420:
1414:
1410:
1409:
1401:
1386:
1380:
1376:
1372:
1365:
1350:
1344:
1340:
1339:
1331:
1323:
1317:
1313:
1312:
1304:
1302:
1293:
1291:0-7487-5802-X
1287:
1283:
1279:
1275:
1267:
1259:
1257:0-521-31958-7
1253:
1249:
1245:
1238:
1230:
1228:0-7506-5780-4
1224:
1220:
1215:
1214:
1205:
1197:
1191:
1187:
1180:
1172:
1170:0-7487-5802-X
1166:
1162:
1158:
1151:
1143:
1141:0-412-75030-9
1137:
1133:
1132:
1124:
1116:
1112:
1108:
1104:
1100:
1096:
1092:
1088:
1080:
1078:0-471-52621-5
1074:
1070:
1063:
1055:
1051:
1047:
1043:
1039:
1035:
1028:
1024:
1015:
1012:
1010:
1007:
1005:
1002:
1000:
997:
995:
992:
991:
985:
983:
973:
965:
951:
947:
945:
941:
931:
929:
925:
921:
911:
909:
905:
895:
892:
886:Flexural slip
883:
875:
873:
869:
866:(also called
865:
861:
852:
843:
841:
837:
827:
825:
820:
817:
814:
809:
807:
797:
795:
794:
789:
782:
778:
774:
769:
760:
758:
755:
751:
747:
737:
735:
731:
721:
719:
715:
704:
692:
684:
676:
672:
669:
660:
656:
651:
642:
640:
636:
626:
624:
616:
613:
610:
606:
603:
601:
598:
595:
592:
588:
585:
582:
578:
575:
574:
565:
562:
559:
556:
553:
550:
547:
544:
540:
537:
534:
530:
527:
526:
518:
513:
505:
497:
491:Types of fold
469:
465:
447:
437:
427:
417:
399:
393:
386:
385:
379:
377:
373:
372:similar folds
369:
361:
356:
347:
345:
336:
334:
330:
323:Fold symmetry
320:
318:
314:
309:
300:
291:
289:
285:
281:
277:
268:
259:
245:
243:
239:
234:
232:
228:
224:
223:axial surface
215:
211:
209:
205:
201:
197:
193:
189:
185:
180:
178:
174:
165:
154:
150:
146:
143:
142:Rainbow Basin
139:
131:
127:
125:
122:e.g. above a
121:
118:
114:
110:
106:
102:
98:
94:
90:
89:igneous rocks
86:
82:
78:
74:
73:pore pressure
70:
65:
63:
59:
55:
51:
47:
44:
40:
36:
28:
23:
19:
2531:
2440:Thrust fault
2129:Large-scale
2100:Inclinometer
2074:Stress field
1960:
1940:
1915:
1886:
1872:
1831:
1827:
1821:
1802:
1779:
1772:
1753:
1750:"Figure 2.6"
1743:
1731:. Retrieved
1727:
1714:
1702:. Retrieved
1687:
1680:
1668:. Retrieved
1654:
1644:
1632:. Retrieved
1625:the original
1596:
1592:
1579:
1567:. Retrieved
1563:the original
1542:
1538:
1528:
1516:. Retrieved
1502:
1491:
1479:. Retrieved
1472:the original
1451:
1447:
1434:
1422:. Retrieved
1407:
1400:
1388:. Retrieved
1374:
1364:
1352:. Retrieved
1337:
1330:
1310:
1281:
1277:
1266:
1247:
1237:
1212:
1204:
1185:
1179:
1160:
1150:
1130:
1123:
1093:(1): 45–62.
1090:
1086:
1068:
1062:
1037:
1033:
1027:
1014:Thrust fault
979:
976:Oil industry
970:
948:
940:stress field
937:
917:
907:
903:
901:
893:
889:
881:
867:
864:flow folding
863:
859:
857:
846:Flow folding
836:country rock
833:
821:
818:
810:
803:
793:sheath folds
791:
788:simple shear
785:
781:Cap de Creus
743:
729:
727:
717:
710:
702:
664:
653:Box fold in
632:
620:
590:
580:
542:
532:
463:
391:
375:
371:
367:
365:
342:
333:asymmetrical
326:
316:
312:
305:
279:
273:
256:
241:
237:
235:
226:
222:
220:
187:
183:
181:
176:
172:
170:
108:
104:
92:
66:
57:
49:
38:
32:
18:
2621:Paleostress
2507:Slickenside
2482:Crenulation
2435:Fault trace
2430:Fault scarp
2420:Disturbance
2405:Cataclasite
2294:Rift valley
2214:Half-graben
2184:Fault block
2169:DĂ©collement
659:Morro Solar
376:dip isogons
360:convergence
329:symmetrical
227:axial plane
58:fold trains
54:deformation
43:sedimentary
2687:Categories
2649:Pure shear
2636:Shear zone
2593:Competence
2477:Compaction
2354:Fracturing
2149:Autochthon
2144:Allochthon
1733:31 October
1704:1 November
1670:31 October
1634:31 October
1569:31 October
1518:31 October
1481:1 November
1424:1 November
1390:31 October
1354:1 November
924:migmatites
860:competence
777:shear zone
757:evaporites
635:rock types
609:migmatites
390:Curvature
368:concentric
288:wavelength
262:Fold shape
177:hinge line
173:fold hinge
113:compaction
2585:Boudinage
2565:Monocline
2560:Homocline
2540:Anticline
2522:Tectonite
2512:Stylolite
2487:Fissility
2464:lineation
2460:Foliation
2324:Syneclise
2269:Obduction
2239:Inversion
2131:tectonics
1864:129424734
1621:129086677
1115:0016-7606
1054:0016-7878
908:thickness
840:laccolith
775:within a
773:mylonites
734:monocline
668:competent
623:homocline
561:Monocline
529:Anticline
471: 3
449: 2
401: 1
313:Isoclines
253:Fold size
238:fold axis
208:concavity
192:curvature
124:laccolith
120:intrusion
93:fold belt
81:sediments
2672:Category
2644:Mylonite
2575:Vergence
2570:Syncline
2472:Cleavage
2397:Faulting
1856:30068680
988:See also
944:rheology
928:cleavage
898:Buckling
806:tectonic
754:Triassic
591:youngest
549:Antiform
543:youngest
539:Syncline
396:Comment
344:Vergence
284:circular
145:syncline
50:"folded"
2545:Chevron
2532:Folding
2377:Fissure
2329:Terrane
2274:Orogeny
2254:MĂ©lange
2189:Fenster
2079:Tension
1836:Bibcode
1601:Bibcode
1547:Bibcode
1456:Bibcode
1095:Bibcode
999:Orogeny
872:glacier
597:Chevron
555:Synform
464:similar
280:cuspate
276:chevron
147:in the
117:igneous
2319:Suture
2304:Saddle
2244:Klippe
2209:Graben
2069:Stress
2059:Strain
1949:
1926:
1920:409–14
1862:
1854:
1809:
1787:
1760:
1695:
1661:
1619:
1509:
1415:
1381:
1345:
1318:
1288:
1254:
1225:
1192:
1167:
1138:
1113:
1083:after
1075:
1052:
813:slumps
661:, Peru
581:oldest
533:oldest
523:Linear
478:< C
466:folds
408:> C
200:trough
75:, and
69:stress
46:strata
2654:Shear
2382:Joint
2264:Nappe
2224:Horst
2219:Horse
1860:S2CID
1852:JSTOR
1724:(PDF)
1628:(PDF)
1617:S2CID
1589:(PDF)
1475:(PDF)
1444:(PDF)
1020:Notes
874:ice.
824:reefs
639:crust
587:Basin
571:Other
480:outer
476:inner
458:outer
454:inner
410:outer
406:inner
387:Class
315:, or
196:crest
184:hinge
151:near
101:fault
2555:Dome
2462:and
2387:Vein
2367:Dike
2299:Rift
2110:Rake
1947:ISBN
1924:ISBN
1807:ISBN
1785:ISBN
1758:ISBN
1735:2009
1706:2009
1693:ISBN
1672:2009
1659:ISBN
1636:2009
1571:2009
1520:2009
1507:ISBN
1483:2009
1426:2009
1413:ISBN
1392:2009
1379:ISBN
1356:2009
1343:ISBN
1316:ISBN
1286:ISBN
1252:ISBN
1223:ISBN
1190:ISBN
1165:ISBN
1136:ISBN
1111:ISSN
1073:ISBN
1050:ISSN
577:Dome
221:The
188:limb
186:and
171:The
39:fold
37:, a
1844:doi
1609:doi
1597:106
1555:doi
1464:doi
1103:doi
1042:doi
621:(A
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